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DEPARTMENT OF THE INTERIOR 

UNITED STATES GEOLOGICAL SURVEY 

GEORGE OTIS SMITH, Director 

Water-supply Paper 338 



SPRINGS OF CALIFORNIA 



BY 

GERALD A. WARING 




WASHINGTON 

GOVERNMENT PRINTING OFFICE 
1915 



DEPARTMENT OF THE INTERIOR 

UNITED STATES GEOLOGICAL SURVEY 

GEORGE OTIS SMITH, Director 



Water -SuppiiY Paper 338 



SPRINGS OF CALIFORNIA 



9^ 



BY 



GERALD A. WARING 




WASHINGTON 

GOVERNMENT PRINTING OFFICE 
1915 



Wwofraph 






a 0F n. 

'^AFT i 1915 



CONTENTS. 



Page. 

Introduction by W. 0. Mendenhall 5 

Physical features of California 7 

Natural divisions 7 

Coast Ranges 7 

Great Central Valley 11 

Lava-covered region 12 

Sierra Nevada 12 

Southeastern desert 13 

Faults 14 

Natural waters 15 

Use of terms ' ' mineral water " and ' ' pure water " 15 

Mineral analysis of water 15 

Source and amount of substances in water 17 

Degree of concentration of natural waters 21 

Properties of mineral waters 22 

Temperature of natural waters ■ 24 

Classification of mineral waters 25 

Therapeutic value of waters 26 

Analyses of California spring waters 28 

Sources of analyses 28 

Conversion of analyses. 29 

Classes of springs 30 

Order of discussion 31 

Hot springs - 32 

Carbonated springs - . . , 155 

Sulphur springs 253 

Saline springs 289 

Magnesic springs 309 

Iron springs 312 

Artesian springs 313 

Large cold springs 326 

Minor perennial springs 333 

Tabulated data 370 

Index 403 



ILLUSTRATIONS. 



Plate I. Topographic map of California., showing locations of springs In pocket. 

II. Geologic map of California In pocket. 

III. Map of California, showing locations of hot, carbonated, and sul- 

phur springs In pocket. 

IV. A, Arrowhead Hot Springs, San Bernardino County; B, Orrs Hot 

Springs, Mendocino County; C, Paraiso Hot Springs, Monterey 

County; D, Wilbur Hot Springs, Colusa County 32 

V. A, Kellys Hot Spring, Modoc County; B, Delonegha Springs, Kern 

County; C, The Geyser, Plumas County 50 

VI. A, Hough Springs, Lake County; B, Harbin Springs, Lake County; 

C, Howard Springs, Lake County 92 

VII. A, Byron Hot Springs, Contra Costa County; B, Klamath Hot 

Springs, Siskiyou County; C, Fetters Hot Springs, Sonoma County. 108 
VIII. A, Calcareous tufa near Shaffer Hot Springs, Lassen County; J5, 

Carbonate deposit of Jordan Hot Springs, Tulare County 124 

IX. A, Travertine ridges near Bridgeport, Mono County; B, Carbonate 

deposit beside Indian Creek, Plumas County 134 

X. A, The Geysers, Sonoma County; B, Casa Diablo Hot Springs, Mono 

County; C, Bumpass Hot Springs, Shasta County 140 

XL Map of Lassen Peak region, California 140 

XII. A, Cooks Springs, Colusa County; B, Tuscan Springs, Tehama 

County; C, Bartlett Springs, Lake County 200 

XIII. A, Jackson Valley Mud Springs, Mendocino County; B, Grizzly 

Springs, Lake County; C, Nelson Soda Springs, Tulare County 242 

Figure 1. Map of The Geysers, Sonoma County 84 

2. Sketch map showing positions of Big Bend Hot Springs, Shasta 

County , 116 

3. Sketch of travertine ridges near Bridgeport, Mono County 134 

4. Sketch map showing positions of springs in Alum Rock Park, Santa 

Clara County 209 

A 



INTRODUCTION. 



By W. C. Mendenhall. 



In 1903 the United States Geological Survey began an investigation 
of the imderground water of Cahfornia, generally with financial coop- 
eration on the part of the State. Since that year ten papers on the 
underground water of the State have been issued by the Survey, each 
representing an investigation that has been completed. The field 
work which is to serve as the basis for two additional papers has also 
been done and the reports are in preparation. Investigations have 
been begun in two other areas in the State and their results will 
eventually be assembled and pubhshed. 

Since a period soon after the inception of the California work those 
responsible for its conduct have realized the desirabihty of a special 
study of the springs, particularly those wliich yield mineral waters 
and wliich are utihzed to a greater or less extent by citizens of the 
State and by tourists as recreation and health resorts. It did not 
become practicable to begin this work until the summer of 1908, 
when Mr. G. A. Waring, who had assisted in some of the earUer 
Cahfornia studies and had investigated for the Survey certain areas 
in southern Oregon and Wasliington, was assigned to the task of 
collecting and assembhng the necessary data. 

California, with an area of 158,000 square miles, is the second 
largest State in the Union. It exhibits wide geographic diversity, 
since it includes the lowest area in the United States — Death Valley, 
276 feet below sea level — and the highest — Mount Whitney, 14,501 
feet above the sea; and accompanying this geograpliic diversity 
there is a corresponcUng range in scenic effects, chmate, and vegetation. 
The records obtained at meteorological stations in the Salton Sink 
indicate a maximum temperature of 130° in the shade, the liighest of 
record within the continental United States, It is probable that 
minimum temperatures on the liigher peaks, hke Mount Whitney 
and Mount Shasta, approach the minimum witliin our boundaries. 
Rainfall records in the most arid sections of the southern deserts of 
the State represent the extreme of aridity in the United States, 
with averages of less than 3 inches per annum and periods of 12 
montlis or more with only traces of rain, whereas the precipitation 

5 



6 SPRINGS OF CALIFOENIA. 

in northwestern California is very heavy, an annual average of close 
to 100 inches being recorded at a few stations in Mendocino and Del 
Norte counties. 

The ircmensity of the area of the State has made the collection of 
the field data required for the report a task of considerable magnitude, 
though its diversity has added greatly to the interest of the work. In 
the original plan it was estimated that two years of field studies 
would prove sufficient. Mr. Waring succeeded in visiting the more 
important locahties during this period, although some of his exami- 
nations were, of necessity, rather cursory. In midsummer, 1910, 
after the completion of the field work and the assembUng of the greater 
portion of his data in manuscript form he was called by the Govern- 
ment of Brazil to take charge of general water-supply investigations 
in the northeastern arid portion of that South American repubhc. 
The task of reviewing, editing, and supplementing in some respects 
th^ results of his studies was thus unavoidably left to others. This 
task was rendered light by the systematic form in which Mr. Waring's 
material was left. 

It was a matter of regret to Mr. Waring, as it has been to those 
associated with him, that the financial hmitations which controlled 
his work made it impracticable to procure the large number of new 
analyses which are particularly important in a paper of this type, in 
which waters of unusual chemical characteristics are discussed. Such 
analyses as are available have been assembled from all possible 
sources and combined with those which were prepared especially in 
connection with this investigation. The result, although it is in 
some respects unsatisfactory, furnishes a basis for a general view of 
the characteristics of the spring waters and serves to permit their 
classification in a general way. Mr. Herman Stabler has reviewed 
the chemical data and rearranged and interpreted the available 
analyses. 

It is hoped that the report, setting forth as it does the results of 
impartial observations upon one of the important present and more 
important prospective resources of the State, will prove of value to 
its citizens as well as to its visitors, and that the assembled material 
will not be without interest to physicians, chemists, geologists, and 
teachers who may have especial need for the information contained 
in the volume. 



SPRINGS OF CALIFORNIA. 



By Gerald A. Waring. 



PHYSICAL FEATURES OF CALIFORNIA. 

NATURAL DIVISIONS. 

As a basis for the discussion of springs and spring waters of Cali- 
fornia a brief outline of the physical features of the State is here 
presented, together with a few notes on the character of the rocks 
and their structure. Such an outhne will in a measure serve to 
explain the topographic and geologic maps (Pis. I and II, in pocket) 
and will indicate in a general way the relations of the facts shown on 
these maps to the various springs. 

Five main physiographic provinces may be recognized in the 
State: (1) The Coast Ranges, (2) the Great Central Valley, (3) the 
lava-covered region of the northeast, (4) the Sierra Nevada, and (5) 
the southeastern desert region. Not all of these provinces are dis- 
tinctly separated from one another; neither do they consist entirely 
of marked topographic or structural features; but they form fairly 
well-defined natural divisions that are convenient in discussing the 
general features of the State. 

COAST RANGES. 

The term "Coast Ranges" is used in the present paper to designate 
the system of mountain ranges between the Great Valley and the 
Pacific, to which the term "Coast Range" has been apphed, with 
different limitations, by several geologists.^ In general, these ranges 
Ue approximately parallel to the coast, but in the areas of more com- 
plex structure a few trend in other directions. To the ridges or 
groups that make up the system many names have been applied. 
The range in the extreme northwestern part of the State, forming the 
divide between the Smith and Klamath River basins and the bound- 
ary between Del Norte and Siskiyou counties, is called the Siskiyou 
Mountains, and the mountains that extend eastward along the course 
of Klamath River are also considered a part of the Siskiyou Moun- 

1 See Fairbanks, H. W., Review of our knowledge of the California Coast Ranges: Geol. Soe. America 
Bull., vol. 6, pp. 73-75, 1894. Lawson has used the term "Coastal system" in speaking of the main por- 
tions of the Coast Ranges, in the report of the California Earthquake Investigation Commission (The Cali- 
fornia earthquake of Apr. 18, 1906, vol. 1, pt. 1, p. 5). 

7 



8 SPRINGS OP CALIFORNIA. 

tains. To the south., trending in general east and west and forming the 
northern boundary of Trinity County, are the Scott Mountains. The 
Trinity Mountains, and, farther south west,the Bully Choop and YoUa 
BoUy mountains, form the eastern boundary of the same county. In 
the southwestern part of Trinity County, along the eastern side of 
Mad River, are the South Fork Mountains. Farther south, in southern 
Humboldt County, an area of sharply cut ridges and canyons, locally 
known as the Wildcat region, forms part of the Mendocino Range. 
A similar system of ridges continues southward through Mendocino 
County, but the mountains forming this portion of the Coastal system 
are not known by a distinctive name. 

The name Klamath Mountains was suggested by Maj. Powell as 
a general title for this group of ranges in the northwestern part of 
the State, and this name has been adopted by Diller ^ in his pubhca- 
tions on the region. These mountains, generally speaking, are less 
than 5,000 feet in elevation, but the higher peaks of Scott and YoUa 
Bolly mountains are more than 7,000 feet above sea level. They 
are composed mainly of slates, schists, and granitic rocks of Triassic, 
Carboniferous, or, perhaps, earlier geologic age,^ and of a younger 
series of altered sandstones and shales associated with cherts and 
schists that probably belongs to the Franciscan formation, which is 
beheved to be either Jurassic ^ or Lower Cretaceous in age.* The 
Franciscan sedimentary rocks generally contain intrusive masses of 
serpentine and of basaltic material that usually has the character 
of a diabase. These intrusive rocks are so commonly present in 
the Franciscan that they may be regarded as characteristically 
associated with that formation, although they do not properly form a 
part of it. Granitic rocks and gneisses are also exposed among the 
altered sediments of the northern Coast Ranges and are thought to 
be in part intruded in the sediments. The sedimentary rocks 
throughout the Klamath Mountain region have been sharply folded, 
and their structure is intricate and complex, but it is not known in 
detail because only reconnaissance studies have been made of these 
rocks. 

A few sulphur springs issue from the schists of this region, occa- 
sional salt springs yield flows of slight amount from the slates and 
shales, and a few small carbonated springs are scattered through the 
areas of granitic rocks. 

In Mendocino, Lake, and Sonoma counties, south of the region 
that is considered to compose the Klamath Mountains, there are 

1 Diller, J. S., Tertiary revolution in the topography of the Paciiic coast: U. S. Geol. Survey Fourteenth 
Ann. Report, pt. 2, pp. 404-405, 1894. 

2 Diller, J. S., op. cit., PI. XLV. 

sBranner, J. C, Newsom, J. F., and Arnold, Ralph: U. S. Geol. Survey Geol. Atlas^ Santa Cruz folio 
(No.l63),p. 2, 1909. 

^Lawson, A. C, The California earthquake of Apr. 18, 1906: Rept. State Earthquake Investigation 
Conini.,vol. l,pt. l,pp. 7-«,190S. 



PHYSICAL FEATURES OF CALIFORNIA. 9 

other irregular but lower ranges. Peihaps the most distinctive of 
these is the St. Helena Range, which forms the boundary between 
Lake and Sonoma counties. The northern and western ranges in 
these counties are composed largely of altered sedimentary rocks 
that probably belong to the Franciscan formation. Glaucophane 
schists and serpentme are associated with them. The age of other 
altered sedimentary rocks in this area has not been determined. 
Some geologists believe that they belong to the Franciscan forma- 
tion, others believe that they are of Lower Cretaceous age and are a 
part of the formation known as the Knoxville from the type locality 
near Knoxville in Napa County, where they are well exposed. As 
both series of sediments are more or less altered they are not differ- 
entiated on the geologic map (PL II, in pocket). 

In Napa County and the southern part of Lake County several 
peaks and ridges are formed of lava that is probably of Tertiary age. 
This lava overlies the altered sediments, and tuffaceous phases of it 
form prominent cliffs at a number of localities. Numerous carbon- 
ated springs of slight flow issue in this region north of the bay, both 
from the sedimentary rocks and from the lavas, and hot springs exist 
at several places. A few sprmgs of noticeably sulphureted water 
have also been examined but are less numerous and less important 
than those of the carbonated type. 

The Coast Ranges between San Francisco and Los Angeles in gen- 
eral trend nearly parallel with the coast. Among them are the Santa 
Cruz Mountains, which lie along the boundary between Santa Clara 
and Santa Cruz counties; the Diablo Range, which separates San 
Joaquin, and San Benito valleys; and the Gabilan Range, which lies 
between San Benito and ^Monterey counties. The Santa Lucia Range 
forms a mountainous region in southern Monterey and northern San 
Luis Obispo counties, and the Temblor Range is in eastern San Luis 
Obispo and western Kern counties. The San Rafael and Santa 
Ynez mountains are in Santa Barbara County and trend in a general 
northwest direction. In Ventura County, Pine Mountain and, east 
of it, the Topatopa Mountains, extend in general from east to west, as 
do the Santa Susana Mountains, in western Los Angeles County. The 
Tehachapi Mountains trend northeastward through southern Kern 
County, and although bridging the gap between the Coast Ranges 
and the Sierra are, because of their rock types and structure, properly 
regarded as belonging to the latter rather than to the former. Most 
of the Coast Ranges south of San Francisco Bay are only 2,000 to 
3,000 feet in elevation, but the highest parts of the Tehachapi Moun- 
tains attain heights between 5,000 and 6,000 feet. For the most part 
these Coast Ranges south of San Francisco Bay are composed of un- 
altered sedimentary rocks of Cretaceous and Tertiary age, but con- 
siderable masses of the Franciscan formation persist southward from 



10 SPEINGS OF CALIFORNIA. 

San Francisco Bay, and granite is exposed at several points. Lime- 
stone and slate also outcrop at a few localities near the coast. 

The rocks that make up these ranges are usually folded into anti- 
clines (archlike folds) and synclines (inverted arches). They are 
also faulted in many places, so that their structure is complex. The 
deposits of oil and of natural gas in these ranges and about their bor- 
ders are of great economic importance, and their occurrence is closely 
related to the structure of the rocks. 

A few carbonated springs and some scattered sulphur and saline 
springs are found in the unaltered sediments. In the arid region in 
the southern part of the Temblor Range, along the southwest side of 
San Joaquin Valley, a number of surface springs that yield small 
amounts of water of poor quality are of local importance because 
they furnish watering places for travelers and for stock. The springs 
of chief geologic interest in this region are, however, thermal, and like 
the others they issue mainly from the unaltered sediments. 

The representatives of the Sierran and Coastal systems south of 
the Tehachapi are not so clearly differentiated nor so readily recog- 
nized as in middle California. At the southern end of the San 
Joaquin Valley the Sierra swings westward as the Tehachapi Range, 
separating the Great Valley lowland on the northwest from the desert 
lowland on the southeast. Mount Finos, the culminating point on 
the divide between the Cuyama, the San Joaquin, and the southern 
Santa Clara drainage systems, lies at the center of a mountain 
group in which Coast Range and Sierran characteristics are both 
displayed. Extending southeastward from this central point, the 
S.an Gabriel, San Bernardino, and San Jacinto mountain groups 
resemble the Sierra, while the Santa Monica and the Santa Ana 
mountains are properly regarded as of the Coast Range type. The 
Santa Ana Mountains, however, merge 'southward with the spurs of 
the San Jacinto and Santa Rosa groups, to form the Peninsula 
Range,^ which extends southward through San Diego County and 
forms the backbone of the peninsula of Lower California. This range, 
although lower than the Sierra, closely resembles it in geologic and 
physiographic characteristics. 

Moderate altitudes are attained in these southern groups. Mount 
Pinos is about 9,000 feet high; San Antonio and San Jacinto peaks, 
the culminating points respectively in the San Gabriel and the San 
Jacinto mountains, are each more than 10,000 feet in elevation; 
and San Gorgonio, the highest point south of the Sierra, in the 
San Bernardino Mountains, is nearly 11,500 feet above sea level. 
Those of the southern mountains which have been described as be- 
longing to the Sierran type are composed mainly of granitic and 

'Fairbanks, H. W., Geology of San Diego County: California State Mineralogist Eleventh Rept., 
p 76, 1893. 



PHYSICAL FEATURES OF CALIFORNIA. 11 

highly altered metamorphic rocks, although limestones and quartz- 
ites, only slightly altered, occur in considerable masses in the San 
Bernardino Mountains. The rocks in the Coast Range types of 
mountains, on the other hand, are usually slates, shales, sandstones, 
and conglomerates, ranging in age from Triassic to late Tertiary or 
Pleistocene. A fringe of these later sediments lies along the Pacific 
border of the Peninsula Range in San Diego and Orange counties, 
and a similar belt encircles and probably underlies the Colorado 
Desert at the eastern base of this range. 

GREAT CENTRAL VALLEY. 

The Great Central Valley of California, about 16,000 square miles in 
area, includes the Sacramento and San Joaquin valleys, and as its 
name indicates, it occupies a central position in the State. The north 
end of Sacramento Valley is near Redding, where, at an elevation of 
about 600 feet, the lowland along Sacramento River is about 10 miles 
wide. The valley increases in width southward to about 20 miles at 
Red Bluff and 40 miles at Willows, and it continues at approximately 
the latter width to Suisun Bay, into which the Sacramento discharges. 
The broad lowland continues southeastward from Suisun Bay as San 
Joaquin Valley. Its width is only about 30 miles in the northern 
portion, in the vicinity of Stockton, but increases to about 60 miles 
at Hanford. Thence it narrows again to its south end at the base of 
the Tehachapi Mountains, where the valley floor is about 1,200 feet 
above sea level. 

The Sacramento Valley drains through Sacramento River and its 
tributaries into Suisun Bay and thence to the Pacific. The northern 
part of the San Joacjuin Valley also drains out through San Joaquin 
River, but the more arid southern section is an inclosed basin. A low 
alluvial divide that is formed by the delta of Kings River separates the 
drai*nage of the southern half from that of the northern. The Tulare 
basin, whose lowest point is occupied by Tulare Lake, receives a part 
of the drainage from Kings River and all excess waters from the valley 
tributaries south of it. Tliis fluctuating lake, wliich occasionally dries 
up entirely, is merely a great evaporating pan, from whose surface 
the excess waters from Kings, Kaweah, Tule, Kern, .and other rivers 
pass into the atmosphere. 

The only notable interruption in the surface continuity of the Great 
Central Valley is formed by Marysville Buttes, a volcanic mass in the 
central part of Sacramento Valley. The valley surface is almost en- 
tirely covered by alluvium, but unaltered fresh-water and marine 
sediments form most of its bordering slopes and outlying hills, although 
east of the middle portions of both the Sacramento and San Joaquin 
valleys the alluvium of the valley directly overhes the granitic and 
metamorphic rocks of the Sierra. Along the northeastern border of 



12 SPRINGS OP CALIFORNIA. 

Sacramento Valley there is a considerable area of lava agglomerate 
and tuff that has been described by Diller ' as the Tuscan tuff. It is 
considered to consist of volcanic material that was deposited in fresh 
water and hence is shown on the geologic map (PI. II, in pocket) as a 
sediment, but in some places it closely resembles a lava. 

There are very few springs in the Great Valley. Sulphur water 
seeps out at a few places along stream channels, and salt water issues 
in perhaps three or four localities, while a few springs that are not 
noticeably mineralized issue along its eastern margin. 

LAVA-COVERED REGION. 

The lava-covered region forms an extensive area in the northeastern 
part of the State. Its western boundary is formed approximately by 
Sacramento River and by Shasta River, a tributary of the Klamath^ 
The southern boundary extends nearly east and west past the southern 
base of Lassen Peak; the northern and eastern limits are beyond the 
boundaries of the State. The central and northern portions of the 
lava mass form a plateau that is between 4,000 and 5,000 feet in eleva- 
tion. In the northeast the Warner Mountains reach an altitude of 
8,000 feet; on the south Lassen Peak rises to a height of more than 10,000 
feet; to the west Mount Shasta towers to an elevation of 14,380 feet. 
Practically all of this region is covered with lava, which is probably of 
Tertiary and later geologic age. In a few places there are lake-bed 
deposits of partly consohdated sands and clays, and areas of alluvium 
form occasional patches of meadow and valley land. 

A number of hot springs issue in the eastern part of this lava region 
and in the neighborhood of Lassen Peak; in the western portion there 
are many carbonated springs; and in the western and central portions 
are several large cold springs. 

SIERRA NEVADA. 

The Sierra Nevada, the dominating physical feature of the State 
and one of the most imposing mountain groups of the United States, 
extends east of south from the southern base of Lassen Peak to Tejon 
Pass. In the main it forms a great single range which rises in a long 
gentle slope eastward from the Great Central Valley to its crest, and 
thence descends abruptly to the desert region at its eastern base. 
Although as a whole its western side forms a comparatively uniform 
slope that is known to geologists as the Sierran peneplain, in detail it 
departs far from the character of a plain. Numerous peaks form 
prominent irregularities, though their summits conform approximately 
to the mean slope of a peneplain. Deep canyons score this surface 
in a westward direction and further add to the ruggedness of its 
detailed character. In its northern section the crest of the range 

1 Diller, J. S., Geology of the Lassen Peak district: U. S. Geol. Survey Eighth Ann. Kept., pt. 1, 
pp. 422-424, 1889. 



PHYSICAL FEATURES OF CALIFORNIA. 13 

reaches an elevation of 9,000 to 10,000 feet and rises southward to 
its cuhninatiou in Mount Whitney, at an elevation of 14,501 feet. 
Thence the elevation decreases southward to Tehachapi Pass. 

In its northern and western parts there are large areas of more or 
less extensively altered sedimentary and igneous rocks that have 
yielded a great amount of gold and are known as the auriferous series. 
These rocks are associated with intrusive granitic material that 
makes up the larger portion of the range. Lava of Tertiary age 
overlies a considerable area in the north, but farther southward the 
range is composed almost wholly of granites and allied rocks whose 
massive and homogeneous character has caused it to weather into 
prominent barren, dome-shaped mountains. 

A number of small carbonated springs issue in several general 
groups in the Sierra. There are also a few hot springs in isolated 
localities and a number of cold perennial springs that yield large 
flows. 

SOUTHEASTERN DESERT. 

The southeastern desert region of California consists of a number 
of detached mountains and ranges which are separated by arid 
valleys and by flat ai-eas of desert alluvium. In the northern section 
the ranges trend in general north and south. The White Mountains, 
in the southeastern part of Mono County and northern Inyo County, 
and the Inyo Mountains, farther west, have this trend. Between 
Owens Lake and the eastern border of the State there are several 
approximately parallel ranges which also extend from north to south. 
The Coso Range, which lies southeast of Owens Lake, is composed 
mainly of granitic rocks, though lava covers a small area in its central 
part. The Argus and the Slate ranges, which lie farther east, are 
composed largely of granitic rocks and altered sediments, as is also 
the Panamint Range, which borders the western side of Death Valley. 
The Amargosa Range, on the eastern side of the valley, includes the 
Grapevine, Funeral, and Black mountains, whose rocks are mainly 
quartzite, altered limestone, and other altered sediments. The Kings- 
ton Range lies in the northeast corner of San Bernardino County, and 
appears to have the same composition as the desert ranges farther 
north. To the south, in San Bernardino, Riverside, and Imperial 
counties, are a number of isolated ranges that appear to bear little 
relation to one another. Most of these are composed of granitic 
material, others are largely quartzite and other altered sediments, 
and still others are of lava. Elevations of 3,000 to 10,000 feet are 
reached by most of these mountain masses, the highest points being 
in the White Mountains, which are but little lower than the Sierra, 
and in the Panamint Range, where Telescope Peak attains an eleva- 
tion of 11,045 feet. 



14 SPRINGS OF CALIPOENIA. 

Among the valley areas the Colorado Desert, in the southern part 
of the State, and the Mohave Desert and Death Valley region farther 
north, are the principal subdivisions. 

The Colorado Desert, an abandoned and dried-out portion of the 
valley of the Gulf of California, is a great basin whose sides slope 
gently to the lowest point, 273 i feet below sea level, in Salton Sink. 
The Mohave Desert is a broken desert area of indefinite boundaries, 
lying mainly between the southern Sierra, the San Bernardino Moun- 
tains, and Colorado River. Death Valley, lying north of Mohave 
Desert, in Inyo County, is one of many similar arid valleys in south- 
eastern California and southwestern Nevada and is the lowest point 
on the continent, being 276 feet below sea level. There are relatively 
few springs in this southeastern region that are worthy of note, 
except as their scarcity gives all sources of water in desert areas 
peculiar value. A few hot springs in the northern portion are the 
ones of chief geologic interest, while several artesian springs in the 
Colorado Desert are of considerable economic value. There are also a 
few saline springs that are of interest, while many surface springs of 
slight flow are of local importance to travelers as watering places. 

FAULTS. 

Several of the principal structural features in the State are related 
to faults, and these features also appear to be the most prominent 
ones associated with the springs, especially the hot springs. Of the 
major fault lines that have been traced in the State the San Andreas 
fault forms one of the principal zones of displacement, and is the one 
along a portion of which the movement took place that caused the 
earthquake of April 18, 1906. As a structural feature it extends from 
Humboldt County southeastward a distance of 600 miles to the 
Colorado Desert, and is marked throughout the greater part of this 
distance by long, trough -like valleys and steep mountain slopes. 
Another great fault extends along the eastern base of the Sierra. 
Displacement that took place along a portion of it in 1872 produced 
the Owens Valley earthquake of that year. The San Jacinto fault 
extends along the western base of San Jacinto Mountains. Along it 
also displacement has taken place within recent years, the latest 
movement having caused the San Jacinto earthquake of December 
25, 1899. Other fault lines are shown on Plate III (in pocket), and 
still others that have not been traced probably exist in the Sierra and 
the northern Coast Ranges. Their close relation to the hot springs 
of the State is shown on Plate III by the proximity of the springs 
to the fault lines, and the relation of the individual springs to fault 
lines is mentioned in their descriptions. This map was originally 
prepared for reproduction on a smaller scale, and the positions of a 
few of tlie symbols showing springs are therefore less accurate than 
those on Plate I. 



SPRINGS OF CALIFORNIA. 15 

NATURAL WATERS. 
USE OF TEBMS "MINERAL. WATER" AND "PURE WATER." 

No natural water is chemically pure, even rain water containing 
notable amounts of dust, ammonia, and, especially near the coast, 
of saline material. All natural waters may therefore be said to be 
mineral waters. The terms pure and mineral are often used, however, 
to indicate the suitability of a water for some particular use. For 
example, a water considered for a municipal or industrial supply is 
called "pure" if it does not contain objectionable amounts of foreign 
matter. As waters with a markedly mineral taste and all waters 
bottled and sold as drinking water, regardless of their mineral content, 
are customarily termed mineral waters, it follows that a mineral water 
may be so called because it is notably free from mineral or other 
foreign ingredients. 

To a greater or less degree water dissolves practically every sub- 
stance with which it comes in contact. Temperature and pressure 
and the presence of dissolved matter greatly affect the solvent power 
of water, tending to increase or to decrease it. As natural waters 
encounter many minerals in their journeys through and over the 
ground, nearly all waters contain many mineral substances, though 
comparatively few of these substances are present in relatively 
large amount. Furthermore, many waters are saturated with respect 
to some of the less soluble minerals, but a natural water that will 
dissolve no more of any mineral is rare. 

MINERAL ANALYSIS OF WATER. 

To make a mineral analysis of water is to determine the propor- 
tions of the various mineral substances it holds in solution. The 
analyst is unable to determine what chemical compounds have been 
dissolved by the water, nor can he ascertain by the customary 
methods of analysis, what compounds, if any, exist in the solution. 
His work is limited, in the main, to the determination, by indirect 
methods, of certain roots or portions of compounds, known as radicles. 
On account of the indirect methods employed some of the radicles 
reported in analyses can not definitely be stated to be such, but are 
merely conventional terms for expressing the results of some chemical 
reaction in which several radicles may have taken part. With all its 
uncertainties, however, the statement of a mineral analysis of a 
water is a representation of the composition of the water solution, 
and from this statement can be inferred with a considerable degree 
of accuracy much of the story of the water's journey through and 
over the earth, and the effects that may be expected in various uses 
of the water. 

In conformity with tlie modern form of expression the analyses 
are presented in this paper in terms of the radicles, the proportions 



16 



SPRINGS OF CALIFORNIA. 



being expressed in parts per million by weight and parts per million 
of reacting value. The principal radicles reported are listed below: 

Positive and negative radicles. 



Negative. 

Strong-acid: 

Sulphate SO4 

Chloride CI 

Bromide Br 

Iodide -. I 

Nitrate.. NO3 

Weak-acid and hydroxide : 

Carbonate CO3 

Sulphide S 

Phosphate PO4 

Metaborate BOg 

Arsenate ASO4 

Hydroxide^. OH 



Positive. 

Alkali: 

Sodium Na 

Potassium K 

Lithium Li 

Rubidium Rb 

Caesium Cs 

Ammonium NH4 

Alkaline-earth: 

Barium Ba 

Strontium Sr 

Calcium Ca 

Magnesium Mg 

Miscellaneous: 

Hydrogen ^ H 

Iron Fe 

Manganese Mn 

Aluminum Al 



To the radicles should be added three other determinations — 
silica (SiOj), and the gases carbon dioxide (CO2) and hydrogen sul- 
phide (HgS) — which are not listed as radicles because they are 
generally beHeved to be present in water in the colloidal state, or as 
dissolved gases, and are customarily so reported. Under certain 
conditions, however, these three substances may also perform the 
function of radicles in the solution. 

In the foregoing list the hydrogen radicle represents acidity due 
to an excess (in reacting value) of strong-acid radicles over basic or 
alkali radicles. The carbonate radicle in many of the analyses 
given in this paper represents merely alkaUnity due to an excess (in 
reacting value) of basic radicles over strong-acid radicles. 

The analyses presented have been taken from various sources, 
where they were expressed in several different forms. The most 
feasible method of unifjdng these statements with reference to car- 
bonate and bicarbonate radicles and carbon dioxide was to report 
all carbonates and bicarbonates as the carbonate radicle. It may bg 
assumed that where carbon dioxide is reported present, sufficient 
so-called ' 'half-bound " carbon dioxide is present to warrant the report- 
ing of all carbonates as the conventional bicarbonate radicle; that 
where carbon dioxide is reported absent, a mixture of carbonate and 
bicarbonate radicles is represented by the carbonate radicle; and 
that where carbon dioxide is not reported, either condition may exist. 



1 Hydrogen (H) =true acid radicle. 



2 Hydroxide (0H)=true basic radicle. 



NATURAI, WATERS. 17 

SOURCE AND AMOUNT OF SUBSTANCES IN WATER. 

In studying tlio springs of California certain kinds of mineralized 
water were noted as occurring constantly with certain kinds of rocks. 
For example, salt springs were noted in areas of marine sediments, 
strongly magnesic s})rings in areas of serpentine, the more noticeably 
iron-bearing waters in areas of crystalline rocks containing iron 
min(M-als, and the most siliceous waters in hot springs that rise 
through granites or acidic lava rocks. This is mentioned in describ- 
ing the individual springs. 

The probable sources of some of the constituents of natural waters 
are indicated in the following paragraphs: 

Silica is present in most waters in relatively small amount, 50 
parts per million being an unusually high proportion. It is con- 
sidered to exist nearly always as colloidal siUca (SiOj), though the 
presence of a silicate radicle is indicated by some analyses. Silica is 
the chief constituent of the earth's crust and its relative insignifi- 
cance in water is accounted for by the fact that it is only slightly 
soluble except in strongly alkaline solutions. 

Iron and aluminum are widely distributed in nature, though much 
less abundant than silica. In most waters iron is present in greater 
proportion than aluminum, but the sum of both seldom exceeds 25 
parts per milhon. They are only slightly soluble except in acid 
solutions and, as might therefore be expected, are most prominent 
in acid waters. A small amount of iron in water may cause rusty 
spots on clothes that are washed in it, and the staining of porcelain 
plumbing fixtures. 

Manganese, barium, and strontium are relatively rare constituents 
of rocks and are seldom present in water in weighable amounts. 

Calcium and magnesium are normally derived from feldspar and from 
magnesian minerals and are among the most abundant and widely 
distributed substances in nature. In most waters the proportion of 
calcium is two to five times that of magnesium, and where magnesium 
is present in relatively large proportion its source is usually evident 
in near-by magnesia-bearing rocks, mainly serpentine. Magnesium 
is also likely to exceed calcium in highly concentrated sahne waters. 
These two substances cause the "hardness" of many waters, and are 
the main constituents of the hard scale deposited in cooking utensils 
and in steam boilers. 

Sodium and potassium are not markedly different from calcium 
and magnesium in abundance and distribution in rocks. Their 
compounds, with few exceptions, are more soluble than those of 
calcium and magnesium, and they are therefore relatively abundant 
in the more highly concentrated waters. Both are probably derived 
35657°— wsp 338—15 2 



18 SPRINGS OF CALIFORNIA. 

maiiily from feldspathic material. Although about equally promi- 
nent in rocks, sodium is present in waters in much greater proportion 
than potassium. Sodium is usually responsible for the foaming of 
steam boilers. 

Lithium is considered a valuable medicinal constituent of water 
but in most waters is present in too small proportion to warrant 
quantitative determination. When present in relatively great 
proportion it is often calculated as the carbonate, chloride, sulphate^ 
or bicarbonate, but 5.3 parts per milhon of lithium carbonate, 6.1 
parts of the chloride, 7.9 of the sulphate, and 9.7 of the bicarbonate, 
each contain only one part per million of lithium. Dole ^ states that 
since the medicinal value is due to the lithium, not to its compounds, 
a person would need to drink 200 tumblerfuls of water that contains 
one part per million of hthium in order to take a medicinal dose of 
this substance. 

Carbonates are prominent constituents of limestones and dolomites 
and are presumably derived primarily from the action of carbon 
dioxide as a carrier of calcium, magnesium, and sodium. Carbon 
dioxide is always present in the atmosphere and is dissolved in con- 
siderable quantity by water. Its presence in excess greatly increases 
the solubility of most of the weak-acid compounds that are the chief 
constituents of common rocks. The carbonates are the dominant 
negative radicles in most waters. 

Sulphate is thought to be usually produced by the complete oxida- 
tion of sulphur. Sulphated aluminic waters may be produced by the 
oxidation of pyrite (an almost insoluble iron sulphide) in the presence 
of moisture, forming iron sulphate, which is soluble. Reaction with 
the clay of shales then results in an exchange of part of the iron for 
aluminum and magnesium. It is believed that calcic sulphated 
waters exchange their calcium for magnesium and sodium in a 
similar manner when they pass through rocks containing magnesium 
and sodium compounds. Free sulphuric acid is present in a few 
natural W'aters, and acts as a vigorous corrosive. 

Sulphide radicles, of which several more complex forms than the 
simple sulphide exist in water, are probably derived in some waters 
from the partial oxidation of sulphur and in others from the reduction 
of sulphates, especially by means of organic matter. 

Chloride radicle is present in nearly all waters, and, since the 
chlorides of the bases or alkalies found in water are very soluble, is a 
prominent constituent of nearly all very highly concentrated waters. 
The chloride radicle in waters is probably derived from the direct 
solution of sodium and magnesium chlorides. 

1 Capps, S. R., Ground waters of north-central Indiana: U. S. Geol. Survey Water-Supply Paper 254, 
p. 251, 1910. 



NATURAL WATERS. 19 

Bromide and iodide radicles are found in a few spring waters. They 
ai-e usually present in saline waters that obtain their mineral contents 
from marine deposits but seldom in great proportion. 

Ammonium and nitrate radicles are usually supposed to be derived 
dii'ectly from organic matter and tlierefore to indicate pollution, but 
they may be derived from salts produced by organic matter and hence 
may not be evidence of direct contamination. They are seldom 
present in mineral spring waters, as these usually issue from uncon- 
taminated rock sources. 

Phosphate radicle is uncommon in spring water, but it may be taken 
into solution from phosphate minerals, such as apatite. 

Borate is also an uncommon constituent in water, but some springs 
contain it in large amount. It is usually accompanied by sodium and 
is probably derived from the solution of borax. 

Boric acid is commonly present in volcanic emanations in many 
parts of the world, and as boron is a rare constituent of rock-forming 
minerals, the presence in areas of volcanic rocks of waters containing 
borate is worthy of especial note in connection with mineral springs.* 

Arsenate is a rare constituent of water, though there are many 
so-called ''poison" springs that are popularly believed to contain it. 
It is seldom present in measurable proportion, but the water of Owens 
Lake, in California, contains 83.8 parts per million ^ of the element 
arsenic. (See p. 304.) This is one of the largest amounts reported in a 
natural water, but it is in a water that contains more than 213,000 
parts of solids per milhon; so if this water were diluted to a more 
nearly normal strength, of, say, 2,000 parts of solids per million, there 
would be less than one part per milhon of arsenic. 

The source of carbon dioxide, the gas of the ''soda-fountain'"' 
beverages, which is also a common dissolved gas in natural waters, 
has been the cause of much discussion. In many lava regions there 
are strongly carbonated springs, and the source of their content of gas 
is plausibly considered to be carbon dioxide that is occluded in the 
underlying rocks, for this gas is known to be one of the prominent 
constituents of the vapors that are given off by volcanoes during 
eruption. The source of carbon dioxide has been treated fully by 
Delkeskamp,^ whose writings have been reviewed by Lindgren.* 

Delkeskamp believes that to some extent the carbon dioxide may be 
derived from inclusions of liquid carbon dioxide in the quartz grains 
of granite and porphyries and be set free by crushing or heat. It is 
also probably generated in some places from limestone (calcium car- 

' See Gale, H. S., The origin of colemanite deposits: U. S. Geol. Survey Prof. Paper 86j pp. 3-9, 1913. 

2 Stone, C. H., and Eaton, F. M., A new analysis of the water of Owens Lake, California: Am. Chem. Soc. 
Jour., vol. 28, No. 10, pp. 1164-1170, 1906. 

3 Delkeskamp, Rudolph, Juvenile and vadose springs: Balneol. Zeitung, vol. 16, No. 5, Feb., 1905. Also 
other papers by the same author. 

i Lindgren, Waldemar, Econ. Geology, vol. 1, No. 6, pp. 602-612, 1906. 



20 SPEINGS OF CALIFORNIA. 

bonate) and other carbonate rocks by the action of acids. The de- 
composition of organic matter also gives ris'> to carbon dioxide. 

Hydrogen sulphide (the gas which gives the "rotten-egg" odor to 
sulphur waters) is beUeved to be sometimes derived by the action of 
organic matter on calcium sulphate, in the presence of carbon dioxide, 
and this seems to be a plausible source for it in many saUne meadow 
and marsh waters. In hot alkahne waters it may be produced by 
the action of steam on metallic sulphides. When present in notable 
amount it is apt to cause corrosion, rotting, and discoloration of 
articles and fabrics left within its reach. 

Organic matter is present in small amount in many waters and is 
probably derived from vegetable material in the surficial layers of 
soil. Several hypothetical compounds so derived, including crenic 
and apocrenic acids, have been calculated by chemists, but it is not 
certain that they actually exist. Beregin is a transparent, gelatinous, 
mucus-like substance, the product of certain algse that grow in ther- 
mal sulphur springs and impart the odor and flavor of flesh broth to 
the water. These algaB are probably the peculiar feature of so-called 
chicken-soup springs. 

Vegetable growths that are characteristic of certain classes of 
waters are found in many mineral springs. Perhaps the most 
noticeable of these are the varieties of algse that live in warm and 
hot springs and especially in sulphur springs. The color and texture 
of the growths vary with the temperature of the water and the 
rapidity of the current, as well as with the variety of the organism 
itself. The following observations by Weed on the algse in Yellow- 
stone National Park illustrate this change.^ 

The general sequence of colors is well illustrated by the occurrence of such growths 
in overflow streams with a constant volume, such as the outlet of the Black Sand [a 
spring in Yellowstone Park]. As the water from this spring flows along its channel 
it is rapidly chilled by contact with the air and by evaporation, and is soon cool 
enough to permit the growth of the more rudimentary forms which live at the highest 
temperature. These appear first in skeins of delicate white filaments which gradually 
change to pale flesh-pink farther downstream. As the water becomes cooler this 
pink becomes deeper, and a bright orange, and closely adherent fuzzy growth, rarely 
filamentous, appears at the border of the stream, and finally replaces the first-mentioned 
forms. This merges into yellowish-green which shades into a rich emerald farther 
down, this being the common color of fresh-water algse. In the quiet waters of the 
pools fed by this stream the algse present a different development, forming leathery 
sheets of tough gelatinous material with coralloid and vase-shaped forms rising to 
the surface, and often filling up a large part of the pool. Sheets of brown or green, 
kelpy or leathery, also line the basins of warm springs whose temperature does not 
exceed 140° F., but in springs having a higher temperature the only vegetation present 
forms a velvety, golden-yellow fuzz upon the bottom and sides of the bowl. This 
growth is rarely noticed in springs where the water exceeds 160° except at the edge 

1 Weed, W. H., Formation of travertine and siliceous sinter by the vegetation of hot springs: U. S. Geol. 
Survey Ninth Ann. Kept., pp. 657-658, 1899. 



NATURAL WATERS. 21 

of the pool. If the basin is tuunel-shapt'i-l * * * with tiaring or saucer-sliaped 
expansion, algse grow in the cooler and shallower water of the margin, forming con- 
centric rings of yellow, old gold and orange, shading into salmon-red and crimson, 
and this to brown at the border of the spring. Around such springs the growth at 
the margin often ftn-ms a raised rim of spongy, stiff jelly, sometimes almost nibber-like 
in consistency, and red or brown in color. 

Creiiothrix is a small filamentous plant that has a gelatinous sheath 
colored by ferric oxide. It grows especially in ground waters that 
contain considerable iron, and is probably the brown flocculent 
material that is fomid in some iron springs. It sometimes causes 
rusty stains on clothing, and when excessive it may clog faucets and 
pipes. 

Sulphuraria is a slender green plant that secretes silica and grows in 
sulphur waters that have a temperature of less than 122°. 

DEGREE OF CONCENTRATION OF NATURAL WATERS. 

It is probable that none of the several ways of reporting water 
analyses conveys to the nontechnical pereon a clear idea how much 
solid matter is present in solution. The amount of any constituent 
stated in parts per million indicates the proportion, by weight, of the 
amount of that constituent to the solution. For instance, if the 
amount of calcium radicle is stated as 210 parts per milhon it is to be 
inferred that each million pounds of the natural water contains 210 
pounds of the calcium radicle. To correlate this form of expression 
with better known values, it may be stated that one heaping tea- 
spoonful of a substance dissolved in one gallon of water represents 
approximately 4,000 parts per milUon; a rounding teaspoonful, about 
2,500 parts; a thimbleful, about 600 parts; and the amount that can 
be held on the point of a penknife, 10 to 20 parts. The minimum 
amount of sohd material in solution that is perceptible to the taste 
varies greatly with the material, and to a less degree but notably with 
the individual. Experiments on taste sensitiveness have been made 
by Whipple,^ and from his tables and from summaries by Dole ^ it 
appears that as small amounts as 2 or 3 parts per milHon of iron are 
distinctly perceptible to some people, while several times as much 
aluminum is barely so. The alkalies and alkaline earths are much less 
readily detected by the taste. About 200 parts per miUion of calcium 
and magnesium render a water noticeably "hard;" but it seems 
probable that the negative radicles (chloride, carbonate, and sul- 
phate), rather than the positive ones, give the distinctive tastes to 
most mineral waters. About 250 parts per million of chloride renders 
a water distinctly "salty." Of the dissolved gases which occur in 

• Whipple, G. C, The value of pure water, pp. 65-67, Wiley & Sons, New York, 1907. 
2Capps, S. R., Ground waters of north-central Indiana: U. S. Geol. Survey Water-Supply Paper 254, 
pp. 237-239, 1910. 



22 



SPRINGS OF CALIFORNIA. 



natural waters, 4 or 5 parts per million of hydrogen sulphide is 
unpleasant to some people. 

The following three analyses of water from Lake Tahoe, California 
(which contains relatively small amounts of dissolved solids), of an 
average sample from Sacramento River above Sacramento (which is 
probably a fair sample of a slightly mineralized river water), and of 
ocean water show the general character of natural waters, both as 
to nature and amounts of dissolved solids. 

Analyses of natural waters of different degrees of concentration. 
[Parts per million.] 



Constituents. 



By 
weight. 



Reacting 
values. 



By 
weight. 



Reacting 
values. 



By 
weight. 



Reacting 
values. 



Sodium (Na) 

Potassium (K)... 

Calcium (Ca) 

Magnesium (Mg) . 
Sulphate (SO4)..- 

Chloride (CI) 

Bromide (Br) 

Carbonate (CO3) . 
Silica (SiOz) 



7.4 
3.3 
9.4 
3.0 
5.5 
2.3 



72.9 



0.32 

.08 
.47 
.24 
.11 



12 

12 

6.7 
18 

7.0 



0.52 

.60 
.55 
.37 
.20 



10,550 

381 

412 

1,294 

2,643 

18,984 

65 

71 



459 
9.7 
20.5 
106 
55.0 
635 
0.8 
2.4 



34, 400 



i. Water from Lake Tahoe, Cal. Analyst, F. W. Clarke. U. S. Geol. Survey Bull. 330, p. 122. 

2. Water irom Sacramento River above Sacramento, Cal. Average of 10 daily samples June 18-27, 1908, 
an average sample for the year. Total solids varied during the year from 80 in May 19-28 to 140 ia Dec. 25-31. 
Analyst, Walton Van Winkle. U. S. Geol. Survey Water-Supply Paper 237, p. 32, 1908. 

3. Ocean water. Mean of 77 analyses. Dittmar, Challenger Reports, Physics and chemistry, vol. 1, 
p. 204, 1884. 

PROPERTIES OF MINERAL WATERS. 

Practically all natural waters contaui dissolved substances that 
give them both salme and alkahne properties. In some waters the 
saline properties are dominant, in others the alkaline, but seldom is 
one group of substance present to the exclusion of the other. In the 
foUowmg paragraphs some of the more important properties of water 
are briefly discussed. The properties of reaction are defined sub- 
stantially as proposed by Palmer,^ and are expressed in per cent based 
on reacting values, the sum of all properties (except tertiary alka- 
linity) being 100. 

Salinity is a property of reaction such as is caused by the solution of 
strong-acid salts. (See table, p. 16.) Primary salinity is salinity 
such as is caused by the solution of strong-acid salts of the alkalies, 
chiefly sodium and potassium chlorides and sulphates; secondary 
salinity, by the solution of strong-acid salts of the alkaline earths, 
chiefly calcium and magnesium chlorides and sulphates; and ter- 
tiary salinity or persahnity by the solution of strong-acid salts of the 



1 Palmer, Chase, Geochemical interpretation of water analyses: U. S. Geol. Survey Bull. 479, 1911. 



NATURAL WATERS. 23 

miscellaneous group of positive radicles, including iron and aluminum 
chlorides and sulphates, and free strong acids. 

Alkalinity is a property of reaction such as is caused by the solution 
of weak-acid salts. Primary alkalinity is alkalinity such as is caused 
by the solution of weak-acid salts of the alkaUes, chiefly sodium and 
potassium carbonates, sulphides, and borates; secondary alkalinity, by 
the solution of weak- acid salts of the alkaline earths ; and tertiary alka- 
linity or subalkaUnity^ by the solution of weak-acid salts of the miscel- 
laneous group of positive radicles, including ' ' free ' ' weak acids. Under 
this term are grouped the colloids sihca, alumina, and iron oxide; the 
gases carbon dioxide and hydrogen sulphide; and other similar sub- 
stances that occupy an unstable position in the water solution and 
which, under favorable conditions, may contribute to one of the other 
properties of reaction. Tertiary alkahnity, because of its rather 
indeterminate value, is not included in the summation of properties 
to the value 100 and is expressed as a per cent of the sum of all other 
properties of reaction. 

Hardness is a property of the water solution caused by the posi- 
tive radicles other than the alkahes. Hardness is the property 
that results in the decomposition of soap. Temporary hardness, 
which is dissipated by boiling, is measured by secondary alkahnity; 
and permanent hardness, which is not dissipated by boihng, is measured 
by secondary salinity and tertiary salinity. 

Carbonated is a term appUed to waters containing the gas carbon 
dioxide. 

Sulphureted is a term applied to waters containing the gas hydrogen 
sulphide, or sulphureted hydrogen. 

Odor in spring water is noticed chiefly in water from sulphur 
springs, where it is produced by hydrogen sulphide, which is a gas 
that has the odor of decaying eggs. The amount of this gas that 
escapes at some springs is so large that it is perceptible at a distance 
of hundreds of yards. A slight oily odor is perceptible in the water 
of a few springs, but the fishy and musty odors that are often notice- 
able in well waters are rarely present in spring waters. 

Color is not nearly so common in spring waters as it is in stream and 
well waters. A very few strongly sulphureted spring waters have a 
clear greenish-yellow color that is probably due to complex sulphides 
in solution. The waters of white-sulphur springs may be opalescent 
or even milky from the finely divided white, allotropic form of sul- 
phur in suspension ; and the waters of blue-sulphur and black-sulphur 
springs are possibly tmted by other finely divided allotropic forms 
of sulphur or by very small amounts of iron sulphide in suspension. 

' The terms persalinity and subalkalinity have been proposed instead of tertiary salinity and tertiary 
alkalinity, for tertiary salinity or persalinity represents more than salinity, being an acid property, whereas 
tertiary alkalinity or subalkalinity is less than true alkalinity. 



24 SPRINGS OF CALIFORNIA. 

Some spring waters are rendered opalescent or slightly milky by finely 
divided silica or calcium carbonate. A few spring waters are ren- 
dered black by iron sulphide in suspension. 

Radioactivity is a property that is possessed by some waters, and 
it has been offered as an explanation of the curative virtues of some 
mineral springs. No acceptable proof of its healing value has been 
made, however, and it has been shown to be a property that is rapidly 
lost.^ In connection with it may be mentioned the electrical or 
magnetic property that is claimed for some waters, chiefly well waters. 
Careful examination, however, has always shown that such prop- 
erty, if present, belongs to the well casing, not to the water, and is a 
magnetized condition that probably has been produced by the 
action of the drill used in sinking the well. 

TEMPERATURE OF NATURAL WATERS. 

The temperature of the water of many springs remains nearly 
constant throughout the year and practically coincides with the 
mean annual temperature of the locality. Springs that are fed by 
melting snow are of course noticeably below the normal tempera- 
ture; others are considerably above it. Observations of the tempera- 
ture in deep mines and deep borings indicate that in regions of 
comparatively uniform and undisturbed rock, below^ the first 50 
feet (in which the underground temperature is affected by seasonal 
variation in temperature of the air), the temperature increases at 
the rate of 1° F. for about each 50 or 60 feet of increase in depth. 
In favorable locaUties this increment may be safely assumed in 
estimating the depth from which the heated water rises. In the 
greater number of places where thermal springs issue, however, this 
increment is valueless as a basis for estimating the depth from which 
the water rises. The high temperature of the water of most hot 
springs can usually be assigned to faults or displacements in the 
rock formations, to volcanic activity, or to chemical action, rather 
than to normal increase of temperature with depth. The rocks 
along fault zones are probably heated considerably above a normal 
temperature by the great pressure and friction that have been 
produced. Water from deep sources passes upward along these 
zones and is additionally heated by contact with the heated rocks. 
In some areas of volcanic rocks there are probably masses below 
the surface that have not yet cooled to a normal temperature, and 
they heat water which comes near them. Chemical reactions — 
notably the oxidation of pyrite — liberate heat and may increase the 
temperature of underground water. 

' Schlundt, Herman, and Moore, R. B., Radioactivity of the thermal waters of Yellowstone National 
Park: U. S. Geol. Survey Bull. 395, 1909. 



NATURAL WATERS. 



25 



Temperature close to the boiling point is found in many springs. 
As the boiUng point decreases with increase in elevation, and as the 
temperature of the water in several springs in California is at or 
near the boiling point although considerably below the usually 
assumed boiling temperature of 212° F., the following table of boil- 
ing points and approximate elevations is given. The boihng point 
also varies with the barometric pressure, but since a variation of 
one-quarter of an inch in the barometric pressure, which is extreme, 
causes a change of only about one-half degree in the boiling point, 
it is not of great importance. Solids in solution increase the boiUng 
point slightly and gases decrease it, but both of these factors are 
negligible in nearly all thermal spring waters. 

The assumption that an increase of 525 feet in elevation causes a 
decrease of 1° F. in the boiling point of water gives approximately 
accurate results. 

Relation of boiling point of water to barometric pressure and to elevation.^ 



Boiling 


Barometric 


Approximate 


Boiling 


Barometric 


Approximate 


point. 


pressure. 


elevation. 


point. 


pressure. 


elevation. 


°F. 


Inches. 


Feet. 


^F. 


Inches. 


Feet. 


185 


17.05 


14, 350 


199 


22.97 


6,825 


186 


17.42 


13, 800 


200 


23. 45 


6,300 


187 


17.81 


13, 250 


201 


23.94 


5,775 


188 


18.20 


12,700 


202 


24.44 


5,250 


189 


18.59 


12, 1.50 


203 


24.95 


4,725 


190 


19.00 


11, 600 


204 


25.46 


4,200 


191 


19.41 


11,050 


205 


25.99 


3,675 


192 


19.82 


10,500 


206 


26.52 


3,150 


193 


20.25 


9,975 


207 


27.07 


2,625 


194 


20.68 


9,450 


208 


27.62 


2,100 


195 


21.13 


8,925 


209 


28.18 


1,575 


196 


21.58 


8,400 


210 


28.75 


1,050 


197 


22.03 


7,875 


211 


29.33 


525 


198 


22.50 


7,350 


212 


29.92 






a Boiling points and barometric pressures taken from Smithsonian physical tables, 3d ed., 1904, p. 170. 
Approximate elevations computed from scale used on aneroid barometers, which gives an approximate 
rise of 525 feet in elevation for a decrease of 1° F. m the boiling point, up to 10,500 feet in elevation, and a rise 
of 550 feet for a decrease of 1° in the higher computed elevations. 

CLASSIFICATION OF MINERAL WATERS. 

Many plans for the chemical classification of waters have been 
proposed. These plans have in general been based on units of 
weight, and, since such units are obscure indices to chemical energy, 
the class names proposed convey little idea of the character of the 
water solution and amount to little more than an enumeration of the 
names of the radicles or supposititious compounds included in ana- 
lytical statements. Palmer's classification ^ is a rational one, express- 
ing the properties of reaction as percentages of their sum, and affords 
a serviceable key to the character of waters. In this paper, although 
any rigid numerical classification is scarcely warranted because many 

> Palmer, Chase, loc. cit. 



26 SPRINGS OF CALIFORNIA. 

of the analyses presented are proximate only, the properties of reac- 
tion are nevertheless tabulated with each analysis to facilitate com- 
parison. 

THERAPEUTIC VALUE OF WATERS. 

The use of mineral waters under the direction of competent physi- 
cians at mineral-spring health resorts and sanatoriums is attended by 
most beneficial results. It must be admitted that one of the chief 
sources of benefit is the change of habits — the throwing off of business 
cares, the relaxation, fresh air, and exercise — that usually accom- 
panies the use of mineral waters at resorts. This change in itself, 
without the associated mineral-water treatment, is sufficient to accom- 
plish many apparently wonderful cures. That the use and misuse of 
waters is accompanied by marked physiological effects is, however, 
well demonstrated. The cases of misuse have been among the most 
instructive examples in hydrotherapy and have given point to the 
lesson that medicines, whether administered as drugs or as mineral 
waters, should be taken under the advice of those who understand 
their physiological effects. Anderson^ says: 

The indiscriminate use of mineral waters, either for drinking or bathing purposes, 
can not be too strongly condemned, for while they look bland and harmless, they are 
potent therapeutic agents which may accomplish much good if judiciously employed 
but may also do much harm and may be followed by serious if not fatal results in 
careless hands. 

Crook ^ says : 

It may be said without fear of dispute that the most frequent as well as the most 
important component of a mineral spring is the water itself. Aside from its absolute 
necessity to the preservation of all forms of life, this agent possesses certain very 
important therapeutic properties. 

Among these properties he mentions the activity of water as a 
diuretic. The copious use of water in many afflictions of the kidneys 
and genitourinary passages is therefore beneficial. Water tends to 
stimulate perspiration in warm weather, thus cooling the body and 
assisting in the reduction of fevers. The use of quantities of water 
also tends to increase intestinal activity and flush out the bowels. 
The foregoing passages indicate in a general way the value of water 
as a therapeutic agent, but for a complete discussion of the manifold 
functions of water in maintaining and improving the health of the 
human system, the reader should consult a physiological treatise. 

The mineral substances in natural waters tend to augment or 
modify the effects of the water in which they are dissolved. The 
scope of this paper does not permit a detaUed discussion of the 

1 Anderson, Winslow, Mineral springs and health resorts of California, p. 13, Bancroft & Co., San Fran- 
cisco, 1892. 

2 Crook, J. K., The mineral waters of the United States and their therapeutic uses, p. 39, Lea Bros. & 
Co , New York and Philadelphia, 1899. 



NATURAL WATERS. 27 

character and amount of those modifications. The following gen- 
eral notes on tlie subject are, however, presented. In preparing 
them free use has been made of the works of Gutmann,^ Anderson, - 
Schweitzer,^ Crook,^ and Bailey.'^ 

1 . Alkaline waters, and especially waters characterized by primary 
alkalinity, are useful to correct acidity of the stomach and therefore 
aUe^date certam forms of indigestion. Such waters have an aug- 
mented diuretic action and are used in the treatment of fevers, 
rheumatism, gout, vesical irritation, and diabetes. 

2. Waters in which sahnity, measured by the chloride radicle, is 
relatively marked stimulate the appetite and have a general stimu- 
lating effect on the organs of digestion, increasing the flow of the 
digestive juices. Waters in which salinity, measured by the sulphate 
radicle, is relatively marked have a cathartic effect; liighly concen- 
trated waters of this type are much used as purgatives. The sahnity 
of waters also serves to augment their diuretic action. Acid waters 
are astringents and are useful in the treatment of relaxed conditions 
of the mucous membrane, especially when characterized by diarrhea 
and dysentery. Such waters are likely to contain relatively large 
amounts of iron and then are markedly tonic. 

3. The free use of waters characterized by a high degree of second- 
ary salinity and secondary alkahnity is beUeved to have contributed 
to the formation of calculi. For this reason water in which primary 
sahnity or primary alkahnity is pronounced is generally to be pre- 
ferred for use in the treatment of the Iddneys or bladder. Waters 
containing lithium are generally supposed to be especially efficacious 
for such use, but a natural water containing sufficient lithium mate- 
rially to affect its character is rare. 

4. Waters sliglitly carbonated are of very common natural occur- 
rence. The carbon dioxide not only serves to augment the solu- 
bility of many mineral substances, but gives the water an agreeable 
taste, aids the flow of saliva, and allays gastric irritation. 

5. Sulphureted waters generally contain the sulphide radicles to 
wliich their value is believed to be in great part due. Under the 
name ''sulphur waters" such solutions are widely used internally 
and for baths. Waters of this type are particularly valuable in the 
treatment of skin diseases, affections of the liver, and chronic malaria. 

6. The concentration of mineral substances probably does not 
materially affect the character of their therapeutic action, but it 

' Gutmann, Edward, Watering places of Germany, Austria, and Switzerland, 1880. 

2 Anderson, Winslow, Mineral springs and health resorts of California, San Francisco, Bancroft & Co., 
1892. 

' Schweitzer, Paul, A report on the mineral waters of Missouri: Missouri Geol. Survey, vol. 3, 1892. 

* Crook, J. K., The mineral waters of the United States and their therapeutic uses, Lea Bros. & Co., 
New York and Philadelphia, 1899. 

' Bailey, E. H. S., Special report on mineral waters: Kansas Univ. Geol. Survey, vol. 7, 1902. 



28 SPRINGS OP CALIFORNIA. 

determines the quantity of the water that should be drunk. It is 
generally believed, however, that the therapeutic action of a certain 
quantity of mineral is most effective when it is administered in a 
relatively large quantity of water. 

7. Hot waters produce more notable effects than cold waters. 

In regard to the temperature of waters used for bathing, it is 
known that a temperature as low as 66° F. reduces the bodily tem- 
perature about 2° within 10 or 15 minutes, reduces the frequency 
of the pulse, and produces a flow of blood to the brain, lungs, kidneys, 
and other internal organs; but after a cold bath of short duration a 
reaction takes place that causes the blood to return to the skin and 
the pulse becomes normal or even shghtly quickened. Water 88° 
to 95° in temperature is considered to be indifferent in its effect on 
the body temperature, but baths at this temperature are considered 
of value in the treatment of nervous debility and sleeplessness. Hot 
baths accelerate the circulation, induce a flow of blood to the surface, 
and increase the quantity of blood in the superficial blood vessels, 
thereby causing congestions and profuse sweating. Such baths are 
beneficial in the treatment of partial paralysis and of rheumatic 
troubles. The high temperature is probably the main element of 
value in mud and sand baths, though the weight of the material may 
help somewhat. 

ANALYSES OF CALIFORNIA SPRING WATERS. 

SOURCES OF ANALYSES. 

Most of the chemical analyses that are given in this report are 
taken from a book by Anderson,^ who made analyses of most of the 
important springs of the State in 1888-89. A few earlier analyses 
that were made by Oscar Loew in connection with the Wheeler Sur- 
vey ^ are available. A number of others have been taken from the 
reports of the California State Mining Bureau, and others have been 
obtained from advertising folders and from private files. A few 
analyses were made by Mr. F. M. Eaton, at Oakland, CaL, for use in 
this report. 

The source of each analysis is given in the tables, so that the hypo- 
thetical forms may be consulted by those who wish. The following 
abbreviations have been used to indicate the principal references, 
and others are self-explanatory: 

Wheeler report Wheeler, G. M., Annual report upon the geographical 

surveys west of the one-hundredth meridian, 1876. 

Winslow Anderson Anderson, Winslow, Mineral springs and health resorts 

of California, 1892. 

1 Anderson, Winslow, Mineral springs and health resorts of California, Bancroft & Co. San Francisco, 
1892. 

2 Wheeler, G. M., U. S. Geog. Surveys W. 100th Mer. Ann. Rept., 1876, pp. 189-199. 



ANALYSES OF CALIFORNIA SPRING WATERS. 29 

6th Oal Sixth report of Oalifornia State Mineralogist, Sacra- 
mento, 1886 (similarly for the other reports). 

U. S. Geol. Survey Bull. 32 Peale, A. C, Mineral springs of the United States: U. S. 

Geol. Survey Bull. 32, 1889. Similar indications 
are given for other publications of the Survey. 

Advertising matter Analysis obtained from advertising literature relative 

to the spring. 

Owner Analysis obtained from the files of the owner of the 

spring. 

CONVERSION OF ANALYSES. 

The tedious work of converting the analyses (most of which were 
originally expressed in hypothetical forms in grains per gallon) to 
ionic forms in parts per million has been largely done by Gertrude E. 
Goodman, to whom credit is due for reducing them to the standard 
form and thus rendering them available for comparison. In this 
work conversion tables prepared for the various salts by R. B. Dole 
from the atomic weights of 1897 (oxygen = 16.00) have been used. 

In amounts of less than 1 part per million by weight two decimals 
have in most analyses been retained; in amounts of 1 to 10 parts, one 
decimal; and amounts greater than 10 parts are expressed in the 
nearest unit. The totals by summation are given as a check on the 
other figures as well as to show the approximate total solid contents. 

"Where sodium and potassium are reported together in an analysis 
the reacting value has been calculated on the assumption that the 
figures given represent only sodium; similarly where calcium and 
magnesium or iron and aluminum are reported together the values 
are assumed to be all calcium or all iron. 

The properties of reaction have in each analysis been made to 
aggregate 100 per cent without tertiary alkalinity, any excess from 
the other properties being combined with this property. 

Temperatures are expressed in degrees Fahrenheit in the text and 
in both Fahrenheit and Centigrade in the analyses. 

A few typographical errors have been corrected by comparing 
analyses that appear in two or more publications. 

The notes concerning the principal characteristics of the waters, 
as shown by the analyses, have been made by Mr. Herman Stabler, 
who also calculated the reacting values and the properties of reaction. 

Many of the analyses report only the most common substances, 
and a few contain questionable figures, but all are believed to show 
the general character of the waters and, in the absence of better 
analyses, are presented as furnishing the best information available 
concernmg the chemical character of the springs. Two or more 
analyses of water from the same spring are given wherever they are 
available, as they afford valuable checks on unusually high amounts 
of certain substances. The widely differing results of analyses of 
water of the same spring by different persons may be ascribed to 
actual differences in the composition of the water at different times. 



30 SPRINGS OF CALIFORNIA. 

Analyses which were originally reported in grams per liter have 
been converted to standard form by assuming that 1 gram per liter 
is equivalent to 1 part per thousand. This assumption is true only 
when the specific gravity of the water under examination is unity. 
As the specific gravity is seldom stated in an analysis, errors from 
this source could not be corrected, but they are small. In an analysis 
of ocean water, for example, which has an average specific gravity of 
1.026,^ this assumption would make recalculated figures too large by 
about 2.6 per cent, but in less concentrated waters the error involved 
is much smaller. Other notes concerning assumptions that were made 
appear as footnotes to the several analyses.. 

CLASSES OF SPRINGS. 

It was found impracticable to discuss the springs of California 
with any regard to order of importance, for this depends on the extent 
to which they are or may be improved. Some of the springs, most 
remarkable from the viewpoint of the geologist or the chemist, were 
in 1908-1910 unused, while those at several large resorts are of 
relatively minor scientific interest. A discussion based on either 
geographic or topographic arrangement was also considered impracti- 
cable, as it would bear no relation to the character of the springs. 
A strictly chemical grouping was not deemed advisable, because 
sufficient analyses are not available for that purpose, and also because 
according to such a classification, springs that are of different char- 
acter according to the popular view, would be brought together. 
The plan of presentation adopted therefore has been determined by 
the most generally recognized characteristics of the springs and 
includes nine groups, which can not, however, be precisely defined, 
for some springs may be placed nearly equally well under two or 
more heads. The groups are characterized as follows: 

1. Hot springs; temperature higher than about 90° F., or 20° 
higher than that customarily fixed as the dividing point between 
thermal and nonthermal springs. 

2. Carbonated springs; contain notable amounts of free carbon 
dioxide. 

3. Sulphur springs; contain notable amounts of hydrogen sulphide 
or other unstable sulphides. 

4. Saline springs; contain notable amounts -of chlorides or sul- 
phates, or both. 

5. Magnesic springs; contain large amounts of magnesium; brought 
together under one heading in order to call attention to their magnesic 
character. 

6. Iron springs; deposit notable amounts of iron; grouped under 
one heading on account of this fact. 

1 Geikie, Archibald, Textbook of geology, 3d ed., p. 35, Macmillan & Co., London, 1893. 



ORDER OF DISCUSSION. 31 

7. Springs of artesian origin; rise in valleys, yield fairly ])in*e, 
warm water and differ in origin from most of the hot s])rhigs. In 
making this class, the customary grouping of the spring waters into 
thermal and nonthermal classes, with 70° F. as the division point, 
has not been followed. Some artesian springs have higher tempera- 
ture than 70°, and some that are locally considered to be warm but 
are probably not of artesian origin have lower temperatures. 

8. Large cold springs; springs of nearly constant flow, whose 
origin is considered to be somewhat different from that of the springs 
included in the next group. 

9. Perennial s})rings; springs of perennial flow but essentially of 
surface origin, or "hillside" springs. It was impracticable to visit 
or to obtain descri})tions of all of the many springs of this kind in the 
State. In the well-watered mountainous sections many compara- 
tively large springs are of little interest because they are so numerous ; 
in the arid districts small springs of simUar character are of much 
greater importance. Although the list of perennial springs is by no 
means complete, attempt has been made to include those which 
are of sufficient importance to have received names; others which 
have not been considered of sufficient importance to indicate on the 
map (PL I, in pocket) are discussed more generally. 

The foregoing classification is conceded not to be logical from the 
usual standpoint, that of the chemist ; for relatively unimportant con- 
stituents, as carbon dioxide or hydrogen sulpliide, may determine 
the heading under which a spring is discussed. It is considered justi- 
fiable, however, in order best to serve one purpose of this paper as a 
popular catalogue of the springs of Cafifornia. 

ORDER OF DISCUSSION. 

As the hot springs are most important, because of the extent to 
which they have been improved as resorts and of their relations to 
the geologic structure, they are first discussed. Witliin this group 
the order is both geologic and geographic. Springs that issue in 
areas of granitic rocks, beginning in the south and proceeding north- 
ward, are first considered ; then those in the older sediments of the 
northern part of the Coast Ranges, next the hot springs in the lava 
fields of the northeastern part of the State, and last those along the 
eastern front of the Sierra and in the desert area to the south. (See 
Pis. I and III, in pocket.) As Plate III was originally prepared for 
reproduction on a smaller ^cale, the positions of a few of the sym- 
bols showing springs are less accurate than those in Plate I. 

The carbonated springs are described mainly in geographic order, 
beginning with the most prominent group and proceeding north- 
ward through the Coast Ranges, and then southward through the 
Sierra. (See Pis. I and III, in pocket.) 



32 SPRINGS OF CALIFORNIA. 

The sulphur springs, most of which issue in the Coast Ranges, are 
described in an order that takes partial account of their present im- 
portance by beginning with those north of San Francisco Bay and 
proceeding northward through the Coast Ranges, then considering 
those in the western part of the State, south from San Francisco, 
next those in the Siskiyous and the Sierra, and finally a few in the 
eastern desert region. (See Pis. I and III, in pocket.) 

The more notable sahne springs are taken up in geographic order 
beginning in the north. Saline springs and salt licks and desert alka- 
Hne springs worthy of special note are then considered, after which 
several magnesic springs and a few iron springs are described. (See 
PL I, in pocket.) 

The artesian springs are discussed in geographic order, beginning 
in the south, where some of the most noteworthy rise; the large cold 
springs are taken up in order from the north, as the most important 
are found in that part of the State. (See PI. I, in pocket.) 

As the perennial springs have no distinctive features that warrant 
their separation into groups, they are taken up in geographic order, 
beginning in the north and proceeding southward through the eastern 
part of the State and then northward through the Coast Ranges. 
(See PL I, in pocket.) 

In the order of discussion of the springs as well as their classifica- 
tion it was found impracticable to adhere strictly to definite rules. 
Although the arrangement does not permit consecutive numbering 
of the springs, the method of numbering by counties is beHeved to 
enable the position of any spring to be readily found on the map 
(PL I). 

HOT SPRINOS. 

ARROWHEAD HOT SPRINGS (SAN BERNARDINO 36). 

Along the western base of the San Bernardino Mountains in southern 
Cahfornia hot springs issue at several places. The largest group. 
Arrowhead Hot Springs, is situated on the granitic slopes about 7 
miles east of north from San Bernardino and about 500 feet above 
the valley land. The approximate position of these springs is marked 
on the mountain side above them by an area of scanty vegetation in 
the shape of an arrowhead several acres in extent (PL IV, A). 
Indian legends associate this pecuUar landmark with the springs, 
and the early immigrants also attached significance to the remark- 
able sign. 

At these springs a hotel and baths were early erected. This hotel 
was burned several years ago and the present structure, a three-story 
building containing 90 furnished rooms, was completed about 1907. 
Very good bathing arrangements are provided and the place is easily 
reached by electric car from San Bernardino. 



HOT SPRINGS. 33 

The springs form two groups situated about 400 yards apart. The 
upper group comprises perliaps half a dozen springs whoso observed 
temperatures range from 110° to 145°. The water is confuied in two 
concrete storage basins that are in part the foundations of the original 
batliliouse, and it is thence piped to the baths and to heating pipes 
tliroughout the hotel, wliich is about 200 yards southwest of the 
basins. The Palm Spring, on the mesa north of the hotel, is in this 
group. The second group hes in a ra\ane to the west and also com- 
prises about haK a dozen springs. Water from one of these is pumped 
to the storage basins at the upper group to augment the supply for 
the hotel. The hottest water is in the spring known as El Penyugal, 
in the lower group. Tliis spring is surrounded by a concrete basin 
and the water is used for drinking. A temperature of 187° was re- 
corded in the basin and in samphng for one of the analyses the basin 
was drained and a temperature of 202° registered. Tlie spring dis- 
charges perhaps 15 gallons a minute. Granite Spring is on the mesa 
on the west side of Penyugal Canyon. 

Tlie total yield of the Arrowhead Hot Springs is hard to estimate, 
l)ut it is probably not far from 50 gallons a minute. 

Water from a cool spring, Fuente Frio, situated about a quarter of 
a mile north of the hotel, was placed on the local market as a table 
water during 1909. Agua Fria is the water of Cold Canyon, at the 
head of the pipe hne leading to the main reservoir on the high mesa 
north of the hotel. Analyses of several of the springs are given on 
page 34. 

WATERMAN HOT SPRINGS (^^SAN BERNARDINO 36). 

About three-fourths mile west of Arrowhead Hot Springs smaller 
hot springs rise from fissures in the granite on the eastern side of 
Waterman Canyon. These springs have been used to some extent 
for batliing, but when visited in 1908 the accommodations had evi- 
dently not been kept in repair for several years and there was only a 
slight flow of water from a small marshy area and a pool beneath a 
bank at the creek side. An analysis of the water of the only spring 
that has been walled in is tabulated with analyses of the Arrowhead 
Hot Springs. 

35657°— wsi> 338—15 3 



34 



SPRINGS OF CALIFOENIA. 



CN O O GO O 




^t^ CS (D . ^ ^ -(^ 

oOrt Ca PS •-AT 

^- 03 >-._] S . . >.,'-' „ 

SBB*^ d ^ ^+^tf 

^^^5 IB .^'^ 

C3 (33 03 ti<J S.2 . ■ 

fn ►« hr, - -*< a n j3 C 



MMbOoS 
S 3 P 2 

1^ >? S Wl._ . „ „ 

— I « -H a '-' 03 3 Mit; 



HOT SPRINGS. 35 

The analyses indicate that the hot springs of this group arc about 
equal in concentration, the total mineral content being so high as to 
render the waters unfit for many uses but suitable for use medicinally. 
The waters are essentially primary saline in character, tertiary alka- 
linity, though not fully reported, being noteworthy. The differences 
with respect to primary alkaUnity and secondary salinity are of 
interest but are not sufficient to affect materially the character of 
the waters. The cool waters are soft and only slightly mineraUzed. 
Primary sahnity, primary alkahnity, and secondary alkaUnity, though 
not fully reported, are prominent. 

WARM SPRING IN LYTLE CANYON (SAN BERNARDINO 34). 

About 13 miles in a direct line north of west from the Waterman 
Springs, in Lytle Canyon, a hot spring forms a pool in the creek bed. 
The water was at one time used for bathing and the place was known 
as Tyler's Bath. It is now unimproved, however, the flow is small, 
and the water is only about 90° in temperature. A qualitative test 
of the water from this spring was made in 1876 by Loew,^ who found 
it to contain 568 parts per milUon of solids in solution. 

WARM SPRING AT BALDWIN LAKE (SAN BERNARDINO 33). 

Baldwui Lake is a small intermittent water body at the upper end 
of Bear Valley, in San Bernardino Mountains. In a marsh at the 
western end of the lake warm water rises m a pool about 20 feet in 
diameter and has been used to some extent for bathmg, but as the 
flow is slight and the temperature of the water is only 88° it has not 
become important. 

HARLEM HOT SPRING (SAN BERNARDINO 37). 

Hot water formerly issued at Harlem Hot Spring on the alluvial 
slope about 2 miles below the base of the San Bernardino Mountains. 
A well casing has been sunk in the former spring and the water is 
pumped for bathing, and in summer for irrigation also. During 
periods following seasons of abundant rainfall the well overflows, 
but the water level usually stands a few feet below the smiace. 
The property is beside an electric car line and is only a few minutes' 
ride eastward from San Bernardino. It has been made a recreation 
and picnic ground and the water supplies a swimming plunge and 
tub and mud baths. A partial analysis of the water, which has a 
local market as a table water, is tabulated beyond, with that of water 
from Urbita Hot Springs. Primary salinity is dominant in both 
waters. 

1 Loew, Oscar, U. S. Geog. Survej-s W. 100th Mer., 18T6, p. 196. 



36 



SPRINGS OF CALIFORNIA. 



URBITA HOT SPRINGS (SAN BERNARDINO 38). 

About 1 mile south of San Bernardino a recreation park known as 
Urbita Hot Springs has been built about a group of artesian wells that 
yield thermal water. This water supplies a swimming plunge, tub 
baths, and a small lake. The warmest well yields about 200 gallons 
a minute of mildly sulphureted water that is said to have a tempera- 
ture of 106°. The following partial analysis shows that, like the 
water at Arrowhead and at Harlem springs, it is not highly mineral- 
ized, but small amounts of sulphur and iron constituents in the water 
cause it to stain the enameled bathtubs: 

Analyses of wate)' from Urhita Hot Springs and Harlem Hot Spring, San Bernardino 

County, Cal. 

[Analyst, E. W. Hilgard. Authority, advertising matter. Constituents are in parts per million 

by weight.] 



Urbita. 


Harlem. 


Domi- 


D m i - 


nant. 


nant. 





(?) 








Small. 


(?) 


Small. 


Small. 


Present. 


Present. 


80 


60 


310 


260 


25 


90 


415 


410 


133 


144 


21 


10 


42 


16 


114 


90 



Properties of reaction: 

Primary salinity 

Secondary salinity 

Tertiary salinity 

Primary alkalinity 

Secondary alkalinity 

Tertiary alkalinity 

Residue: 

Combined water 

Soluble in water 

Insoluble in water 

Portion soluble in water: 

Sulphate (SO4) 

Chloride (Cl) 

Carbonate (CO3) 

Chiefly sodium (Na) and potassium (K) 

Portion insoluble in water: 

Silica (Si02) 

Calcium (Ca), magnesium (Mg), carbonate (CO3) and sulphate (SO4), chiefly 
calcium 



50 



As has been previously stated, the area along the western base of 
San Bernardino Mountains is a faulted zone. The issuance of hot 
water within this area therefore seems to be due to a fault or struc- 
tural break in the granitic rocks, which allows deep-seated thermal 
water to reach the surface. The abnormal temperature of Harlem 
Hot Spring is possibly due to leakage into the alluvium of heated 
water that rises in the faulted zone. This may also be the source 
of the warm water at the Urbita wells, though there is a bedrock 
area 1 mile south of these thermal wells that may cause under- 
ground alluvial water to rise from a depth sufficient to account for 
its high temperature. Warm water is also obtained from other flow- 
ing wells in this locality. The sulphurous elements of the water from 
the Urbita wells are probably derived from material in the alluvium 



HOT SPRINGS. 37 

rather than from constituents in deep-seated hot water that may 
enter the alhivium. 

FAmVIEW HOT SPRING (ORANGE 1). 

A warm spring or well at Fairview Hot Spring, in the coastal plain 
south of Santa Ana, resembles in occurrence the Harlem and Urbita 
springs. Originally the Fairview Spring was a natural flow, but a 
casing that was sunk to a depth of 700 feet into it has converted 
it into a flowing artesian well. In 1908 a hotel and cottages pro- 
vided accommodations for about 50 people. The water rises with a 
temperature of 96° and suppUes a swimming plunge and tub baths. 
The discharge varies somewhat with the season; in December, 1908, 
it was about 15 gallons a minute. An odorless, inflammable gas rises 
with the water and is burned for cooking and lighting. The water, 
wliich is colored brown, doubtless from organic stain, has been placed 
on the local market for table use under the label "Amberis Water." 
Although the water has a famt oily taste, it is thought to be essen- 
tially ground water that here rises through the deep alluvium which 
forms this part of the coastal plain. Its origin is probably not re- 
lated to the shales of the oil-bearing series of southern California that 
form low hills a mile southward, except as these shales act as an 
underground dam that forces the alluvial water of the artesian basin 
of this region to the surface. 

EDEN HOT SPRINGS (RIVERSIDE 8). 

Along the western base of San Jacinto Mountains are several hot 
springs that have already been mentioned in their relation to the 
San Jacinto fault. At Eden Hot Sprmgs, the northernmost group 
along this fault, about eight small springs rise within a distance of 
100 yards at the base of a steep granitic slope. The water issues less 
than 200 yards beyond the southeastern border of a series of shales 
and sandstones of Tertiary age, in which there are dislocations that 
were probably caused by the uplift of the San Jacinto Range; but the 
springs seem not to be related causally to the sediments. The max- 
imum temperature of the water is about 110°. It is moderately 
sulphureted but does not seem to be otherwise notably mineralized. 
During 1909 water fi'om two of the springs was placed on the local 
market for table use under the labels ''Iron Lithia" and "White 
Sulphur." 

A small resort has been maintained at the place for a number of 
years. In 1908 cottages and tents provided accommodations for 
about 50 people, and a bathliouse and small swimming pool allowed 
use of the water for bathing. 



38 SPRINGS OP CALIPOENIA 

SAN JACINTO HOT SPRINGS (RIVERSIDE 9). 

San Jacinto Hot Springs, formerly known as Relief Hot Springs, 
are situated at the valley edge, 6 miles southeast of the Eden springs. 
About haK a dozen springs here issue from a bank of granitic allu- 
vium and form a marshy area several acres in extent. 

The place has been a resort for more than 20 years, a frame hotel 
and cottages and tents forming a little settlement in a grove adjacent 
to the springs. Besides the usual tub baths there are mud baths that 
use material from the tule marsh. 

The waters are sulphureted and they also taste distinctly alkaline. 
Efflorescent alkaUne salts form in small amounts on the banks beside 
the springs, and the iron and sulphide contents cause the water to 
stain the towels and enameled tubs. The following partial analysis 
of the water that is used chiefly for bathing shows the general char- 
acter of the water, though the several springs differ somewhat in 
chemical characteristics : 

Analysis of water from Black Spring, San Jacinto Hot Springs, Riverside County, Cal. 

[Analyst, E. W. Hilgard (?). Authority, advertising matter. Constituents are in parts per million.] 

Properties of reaction : 

Primary Balinity Dominant. 

Secondary salinity (?) 

Tertiary salinity 

Primary alkalinity (?) 

Secondary alkalinity Prominent. 

Tertiary alkalinity Present. 

Residue : 

Soluble in water 3,770 

Insoluble in water 2, 120 

5,890 

Portion soluble in water. 

Sulphate (SO4) 366 

Chloride (CI) 1,920 

Carbonate (CO3) 30 

Metaborate (BO2) Trace. 

Nitrate (NO3) Trace . 

Sodium and potassium (Na+K), chiefly sodium 1, 454 

Portion insoluble in water : 

SiUca (SiOa) 20 

Calcium (Ca), magnesium (Mg), carbonate (CO3), and sul- 
phate (SO4), chiefly calcium 2, 100 

Hydrogen sulphide (HgS) Present. 

The analysis indicates that the water is highly concentrated, is 
chiefly primary saline in character, and has secondary alkahnity as 
a prominent property. The water is unsuited for industrial or 
asrricultural use. 



HOT SPRINGS. 



39 



RITCHEY HOT SPRINGS (RIVERSIDE 10). 

Ritchey Hot S]")rings, about 5 milos southeast of the San Jacinto 
springs, are also situated near the base of the mountains, but they 
issue along the side of a ra^dne. Six springs, which range in tem- 
perature from 70° to 1 1 1 °, furnish water for domestic use and irrigation. 

Although in 1908 the place had not yet been opened as a public 
resort, a few guests were taken care of during the summer, and sev- 
eral tubs were proAaded for bathing. In a tunnel that has been 
driven into the hillside for a distance of 55 feet a temperature of 82° 
was registered. This unusually high temperature has led to the use 
of the tunnel as a sweat chamber. Gypsum and efflorescent alum 
salts form on its walls and indicate that the tunnel water may be 
mineraUzed to a notable extent by acid constituents. There was 
formerly a sour spring in the ravine above the main group, but at 
the time the place was visited it either had been covered by a land- 
slide or overgrown by vegetation. 

Water from one of the springs was formerly marketed as a table 
water as "Soboba Lithia Water." Its sale was discontinued when 
interrupted by the high-water stage of San Jacinto River in 1904, 
but it was placed on the local market again in 1909. 

The following analysis of this water has been published : 



Analysis of water from ^' lithia^' spring at Ritchey Hot Springs, Riverside County, Cal. 
[Analyst, L. J. Stabler. Authority, advertising matter. Constituents are in parts per million.] 



Properties of reaction: 

Primary salinity 

Secondary saliniity . . . 

Tertiary salinity." 

Primary alkalinity. . . 
Secondary alkalinity . 
Tertiary alkalinity . . 



Sodium (Na) 

Potassium (K)... 

Lithium (Li) 

Calcium (Ca) 

Magn&sium (Mg). 

Iron(Fe) 

Aluminum (Al). . 
Sulphate (SO,).. 

Chloride (01) 

Carbonate (CO3)- 
Silica(Si02) 



Constituents. 



By 
weight. 



55 

71 
Trace. 
1.7 
Trace. 
Trace. 
Trace. 

52 

28 

72 

23 



302.7 



Reacting 
values. 



2.37 

LSI 

Trace. 

.08 

Trace. 

Trace. 

Trace. 

L08 

.79 

2.40 

.76 



Primary alkalinity is the dominant property, and its high percent- 
age is specially noteworthy. Primary salinity and tertiary alkalinity 
are also prominent, though the latter is not fully reported. The rela- 
tively high proportion of potassium is unusual and in the absence of 
confirmation by other analyses should not be given weight. 



40 



SPRINGS OF CALIFORNIA. 



The ra\dne in which these springs issue is steep, with narrow, 
precipitous sides, and the rock exposed is largely a crushed gneiss. 
Recent landslide patches within it also indicate the broken and dis- 
turbed character of this area and furnish local evidence that the 
thermal character of the springs is due to crushing and slipping of the 
rocks. 

PILARES HOT SPRING (RIVERSIDE 7). 

In the channel of San Jacinto River, about 6 miles west of the base 
of the San Jacinto Range, warm water rises and forms a tule area 
several acres in extent. The water was formerly piped to a bath- 
house on the higher land, but in 1910 a hut among the tules formed 
the local bathing place. Though the abnormal temperature of this 
water may be due in part to leakage of deep-seated hot water upward 
through the San Jacinto fault into the alluvium of the valley, it is 
more probable that a buried spur of a granitic ridge that here borders 
the valley acts as a dam and forces alluvial water to the surface from 
a depth sufficient to account for its temperature. A well that was 
drilled a couple of hundred yards west of the spring obtained a warm 
artesian flow. 

PALM SPRINGS (RIVERSIDE 11). 

At Palm Springs, at the southern base of San Jacinto Peak, a rise 
of thermal water tends to confirm the topographic evidence that 
faulting has taken place in this vicinity. The water, which has a 
temperature of about 100°, is used for bathing, and there is a small 
health resort here on the edge of the desert. These are the same 
springs that were formerly known as Aguas Calientes (hot waters), 
and the following partial analysis of the water was early made : 

Analysis of ivater from Palm Springs, Riverside County, Cal. 
[Analyst, Oscar Loew. Wheeler report (1876). Constituents are in parts per million.] 



Temperature 

Properties of reaction: 

Primary salinity 

Secondary salinity 

Tertiary salinity 

Primary alkalinity 

Secondary alkalinity 

Tertiary alkalinity 

Constituents 

Sodium (Na) 

Lithium (Li) 

Calcium (Ca) 

Magnesium (Mg) 

Sulphate (Sd) 

Chloride (01) 

Carbonate (CO3) 

Silica (Si02) 

Hydrogen sulphide (H2S) 



38° C. (100° F.) 

77 



23 

Trace. 

? 



By 
weight. 



Reacting 
values. 



158 
Trace. 
Trace. 
Trace. 
Trace. 

188 

47 

Trace. 



6.87 

Trace. 

Trace. 

Trace. 

Trace. 
5.30 
1.57 

Trace. 



393 



Trace. 



Trace. 



HOT SPRINGS. 41 

MUD VOLCANOES (IMPERIAL 5). 

About 7 miles south of west from Imperial Junetion, in the alluvium 
on the eastern side of Colorado Desert, is an area in wliich vapor and 
hot water vents are numerous. They were submerged by the rise of 
Salton Sea' during 1905-1907, but they will become accessible again 
as the water subsides. They were early visited by Le Conte ^ and by 
"W^atch,^ who describe them as covering a space of about 350 by 500 
yards in an area of blue elay slightly elevated above the desert surface. 
\^apor and hot water issued from numerous low conical mounds in this 
area, and from some of the vents water was formerly thrown to a 
height of 15 to 40 feet. Veatch reports that the water was strongly 
sahne and had a specific gravity of 1,075. He also reported unmis- 
takable evidence of free boracic acid in it. Small amounts of sulphur 
and of a salt that was considered by Le Conte to be sal ammoniac 
(ammonium chloride), were deposited around the vents, and small, 
coral-Hke stalagmites of Ume carbonate were built up by the spray 
from several of the more active springs. In 1905, before their sub- 
mergence by the rising water of Salton Sea, they had become much 
less active, and the locality contained only pools of hot water and 
boiling mud, v4th the usual vapors and sulphur and sahne deposits 
that are characteristic of solfataric regions. There was a smaller 
group of extinct or at least quiescent craters about a mile southeast 
of the main group.* 

These solf ataras are near a row of knobs or small buttes of obsidian, 
pumice, and other varieties of volcanic rock which extend southwest- 
ward from a point about 6 miles west of Imperial Junction, and the 
presence of the hot waters probably represents a final phase of the 
volcanic activity that produced the lava knobs. Since the rise of 
Salton Sea these have become islets and have been made breeding 
places by pelicans. 

A similar but more extensive group of mud volcanoes is found on 
the western sids of Volcano Lake, in Mexico, near the base of the 
Cerro Prieto, about 20 miles south of the international boundary, and 

1 Salton Sea occupies the central part of Colorado Desert. Normallj' it receives only the occasional over- 
flow from distributaries of this river, and it has been dry during a considerable portion of the last half cen- 
tur\'. In the spring of 1905 Colorado River during its flood stage greatly enlarged the intake of acanal which 
supplied irrigation water to a portion of Imperial Valley, and a large part of its discharge, and finally the 
entire stream flowed northward to Salton Sea or Salton Sink. Several attempts were made to close the 
break and stop the destruction that was being wrought in the valley, the river finally being forced back 
to its natiu'al channel in February, 1907. Since the summer of that year the sea has been gradually sub- 
siding as its water has been removed by evaporation. 

2 Le Conte, J. L., Account of some volcanic springs in the desert of the Colorado in Southern California: 
Am. Jour. Sci., 2d ser., vol. 19, pp. 1-6, 1855. 

3 Veatch, J. A., Notes of a visit to the mud volcanoes in the Colorado Desert in the month of July, 1857: 
Am. Jour. Sci., 2d ser., vol. 26, pp. 288-295, 1858. 

* Mendenhall, W. C, Groimd waters of the Indio region, California, with a sketch of the Colorado Desert: 
U. S. Geol. Survey Water-Supply Paper 225, p. 14, 1909. 



42 SPRINGS OF CALIFORNIA. 

60 miles in a direct line south of east from the mud volcanoes near 
Imperial Junction. 

A great fault extends southeastward through San Gorgonio Pass, 
which is eastward from San Bernardino, and this fault is believed to 
continue through Colorado Desert, where physiographic evidence of 
its existence is buried by the valley alluvium. If it does extend 
through the desert, it may have determined the presence of the small 
area of volcanic rocks near the mud volcanoes, and hence they may 
furnish evidence of more extensive geologic phenomena than the lava 
knobs. 

GLEN IVY HOT SPRINGS (RIVERSIDE 3). 

West of the San Jacinto Range another fault has been traced along 
the eastern base of the mountains that border Elsinore and Murrieta 
valleys. Heated waters rise along this fault zone at three localities. 
The most northern of these is at Glen Ivy Hot Springs, which was 
formerly known as Temescal Hot Springs. 

One principal spring, having a temperature of 102° and yielding 
about 15 gallons a minute here issues at the mouth of a ravine in 
which fractured granitic and porphyritic rocks are exposed. Small 
warm springs issue at several other points for half a mile northward, 
but only the one spring is improved. Its water is sulphureted and 
slightly alkaline in taste but is not unpleasant. 

The springs were early known to local settlers, but for a number of 
years they were in private hands, and more recently were the prop- 
erty of an automobile club. In 1908 the place was opened to the 
public. The improvements at that time consisted of a hotel con- 
taining 10 or 12 rooms, a swimming pool, dancing hall, and tennis 
court, all of which were situated in a grove overlooking the valley 
land. 

ELSINORE HOT SPRINGS (RIVERSIDE 5). 

Many small hot springs formerly issued along the northeast side of 
Elsinore Lake. In the early nineties, however, a canal was cut and 
the water of the lake was conducted northward for irrigation, and 
since that time most of the springs have ceased to flow. Hot sul- 
phureted water is still obtained, however, from shallow wells. In 
1888 a large bathhouse was built near the railroad depot; and in 
1908 these baths were still supplied by water pumped from three 
weUs that were formerly springs. A large swimming plunge and tub 
and mud baths were provided, while Lakeview Hotel, under the same 
management, furnished accommodations for about 100 people. 

Partial analyses of water from two of the wells at this resort are 
tabulated on page 43. 



HOT SPRINGS. 



43 



BUNDYS ELSINORE HOT SPRING (RIVERSIDE 4). 

Bundys Elsinore Hot S])riiig' is the luinio of another resort, about 
250 yards north of Elsinore depot. One well at this resort supplies 
warm sulphurated water for drinking and bathing, and a hotel and 
cotta(]:es provide rooms for about 75 guests. A partial analysis of 
this water is tabulated below, with the two from the Elsinore springs: 

Analyses of ivater from Bundys Elsinore Hot Spring and Elsinore Hot Springs, Riverside 

County, Cal. 

[Analyst, E. W. Hilgard. Authority, advertising matter. Coustituents are in parts per million, by 

weight.) 



Properties of reaction; 

Primary salinity 

Secondary salinity 

Tertiary salinity 

Primary alkalinity 

Secondary alkalinity 

Tertiary alkalinity 

Residue: 

Soluble in water 

Insoluble in water 

Combined water and organic matter 

Portion soluble in water: 

Sulphate (SO4) 

Chloride (CI) 

Carbonate (CO3) 

Chiefly sodium (Na) and potassium (K) 

Portion insoluble in water: 

SUica (SiOs) 

Calcium (Ca), magnesium (Mg), sulphate (SO4), and carbonate 

(CO3), chiefly calcium 

Hydrogen sulphide (HoS) 



Dominant. 





Small. 

Small. 

Present. 



Dominant. Dominant 



220 
95 
15 



330 



60 



35 
Present. 





I 
Small. 
Small. 
Present. 



225 
65 
50 






Small. 

Small. 
Present. 



203 
90 
40 



333 



1. Bundys Elsinore Hot Spring. Temperature, 44° C. (112° F.). 

2. Elsinore Hot Springs; original hot spring. 

3. Elsinore Hot Springs; white sulphur spring. 

These partial analyses show the waters to be very similar in con- 
centration and properties. They are soft waters, chiefly primary 
saline in character. 

It is said that previous to the construction of the irrigating ditch 
])ortions of the land near the present hot wells formed quagmires, but 
most of this saturated land has since become dry. Although the 
fault through this region is mapped as passing tlirough Elsinore Lake, 
2 or 3 miles southwest of the springs, the disturbed zone probably 
extends to the eastern edge of the valley and includes the locality 
where the heated waters now rise. The sulphureted character of the 
waters is possibly derived from beds of tule mud through which they 
pass before reaching the surface. 



44 



SPRINGS OF CALIFORlSriA. 



MURREETA HOT SPRINGS (RIVERSIDE 6). 

About 12 J miles in a direct line southeast of Elsinore, on the 
eastern side of Murrieta Valley, a third group of hot springs issues 
along the Elsinore fault zone. The locality is among rolling hills of 
granitic material, that are covered in part by gravels of Quaternary 
age. The heated waters, which are distinctly sulphureted in odor 
and taste, rise at the base of a gravel bluff, on the border of an 
open drainage course. Three springs that rise within 10 yards of 
each other, with a maximum temperature of about 136°, furnish an 
ample supply of water for the resort that has been built up. In 1908 
a frame hotel afforded accommodations for about 75 people, and the 
hot baths were patronized largely for their efficiency in cleansing the 
system from alcoholic poisoning. 

The principal spring is known as Siloam, and one of the others as 
Bethesda, while Ramona Spring is also near by. A small cooler 
mud pool at the base of the slope, some distance beyond the main 
springs, has been occasionally used as a foot bath, and one other cool 
spring of slight flow furnishes a wayside drinking place. The follow- 
ing analysis of the water of Siloam Spring was made a few years ago : 

Analysisof water from Siloam, Spring, Murrieta Hot Springs, Riverside County, Cal. 
[Analyst, C. E. Wagner, Authority, advertising matter. Constituents are in parts per million.] 



Properties of reaction: 

Primary salinity 

Secondary salinity 

Tertiary salinity 

Primary alkalinity 

Secondary alkalinity 

Tertiary alkalinity 

Constituents. 

Sodium (Na) 

Calcium (Ca) 

Magnesium (Mg) 

Iron ( Fe) 

Sulphate (SO4) 

Chloride (01) 

Carbonate (CO3) 

Silica (SiOa) 

Carbon dioxide (CO2) , 

Hydrogen sulphide (H2S) 



weight. 



Reacting 
values. 



249 

9.0 

Trace. 

"3.6 

15 

3G4 

20 

6 47 



10.8 

.45 

Trace. 

.13 

.31 

10.3 

.67 

1.57 



707.6 



52 



2.36(?) 



a Reported as iron; recalculated from re203. 

b Reported as soluble silicate; recalculated from SiOs 



The analysis indicates that this water is essentially a solution of 
common salt in water containing the gases carbon dioxide and 
hydrogen sulphide. 



HOT SPRINGS. 45 

JACITMBA SPRINGS (SAN DIEGO 19). 

The southeastern portion of San Diego County is largely a rolHng 
phitcau-like granitic area. A few miles east of the divide that sepa- 
rates the coastal drainage from that of the Colorado Desert and 
within half a mile of the Mexican boundary are situated the Jacumba 
Springs. In 1908 the water issued at two main points near the chan- 
nel of a small creek. Heavy rains in 1891 and slight earthquake shocks 
in 1892 and 1900 altered the position of the outlets to some extent, 
but the total yield, perhaps 15 gallons a minute, has remained about 
the same. The water is 96° in temperature, is slightly sulphureted, 
and is soft and excellent for laundry and bathing. A small ranch 
and supply store are situated here, and the location of the springs, 
together with the accommodations afforded, make the place a wel- 
come camping spot for travelers between Imperial Valley and the 
coastal settlements. 

The springs were formerly used by a group of Indians, who within 
recent years have made their camp near similar springs a few miles 
to the southeast across the Mexican boundary. They are said to 
designate their present springs as Jacumba and to call those to the 
north Jamati. 

Though no extensive fault is mapped as passing near these springs, 
local faulting, which is indicated by the effect of earthquakes at 
this place, suggests that deep fracturing of rocks here permits the 
escape of thermal water. The springs are only half a mile beyond 
the southern boundary of a small area of lava, however, whose pres- 
ence suggests another cause for the existence of thermal springs in 
this region. 

WARNER HOT SPRINGS (SAN DIEGO 4). 

Warner Hot Springs are situated on the eastern side of Warner 
Valley, near the base of Palomares Mountains in the northern part 
of San Diego County. Half a dozen or more vents here appear in a 
ravine and discharge about 150 gallons a minute of water whose 
maximum observed temperature is 139°. The place has long been 
known to the Indians and Mexicans as Las Aguas Calientes (the hot 
waters) and hence it has been sometimes confused by strangers with 
Palm Springs and with those in the valley of Vallecito Creek (San 
Diego 9, p. 46; Riverside 11, p. 40), which are also known as Aguas 
Calientes. For many years a band of Indians made their home here 
and their mortars for grinding acorns have been worn in the bowlders 
close to the springs. In 1904, however, the Indians were removed 
to the Pala Reservation and since that time a resort has been built 
up at the springs. In 1908 there were about 20 adobe cottages 
and an equal number of tents, the former Indian school building 



46 



SPRINGS OF CALIFORNIA. 



being used as a dining hall. The water was conducted to a wooden 
tank, where it was allowed to cool somewhat, and was thence piped 
to a bathhouse. An analysis of the water, which is noticeably 
sulphureted, follows : 

Analysis of water from main spring at Warner Hot Springs, San Diego County, Cal. 
[Analyst and authority, Curtis and Tompkins (1904). Constituents are in parts per million.] 

59° C. (138° F.) 



Temperature 

Properties of reaction: 

Primary salinity 

Secondary salinity . . . 

Tertiary salinity 

Primary alkalinity. . . 
Secondary alkalinity . 
Tertiary alkalinity . . 



Constituents. 



By 
weight. 



Sodium (Na) 

Potassium (K) 

Lithium (Li) 

Ammonium (NH4) 

Barium (Ba) 

Strontium (Sr) , 

Calcium (Ca) 

Magnesium (Mg) 

Iron (Fe) 

Aluminum (Al) 

Manganese (Mn) 

Sulphate (SO4) 

Nitrate (NO3) 

Chloride (Cl) 

Bromide (Br), iodide (I), and fluoride (F). 

Sulphide (S) 

Carbonate (CO3) 

Metaborate (BO2) 

Arsenate (AsO^) 

Phosphate (PO4) 

Silica (Si02) 



120 

3.3 

Trace. 

.50 



Trace. 

2.6 

.29 

.42 

Trace. 
68 


26 


25 
26 
.64 



1.1 
85 



358. 85 



Carbon dioxide (CO2) 

Hydrogen sulphide (H2S) . 




3.0 



Reacting 
values. 



5.22 
.08 

Trace. 
.03 
.00 

Trace. 
.13 
.02 

.02 

Trace. 

1.43 
.00 
.73 
.00 

1.62 
.87 
.01 
.00 
.03 

2.81 



.00 
.18 



The foregoing analysis contains a detailed report on substances 
for which often no test is made. The primary alkaline character 
of the water — alkalinity due largely to weak acid radicles other than 
the carbonate — and the appearance as primary alkalinity of constit- 
uents generally tabulated as tertiary alkalinity are of special interest. 

The region is one of granitic rocks, and a fault that passes along 
the east side of Warner Valley has been recognized by geologists 
who have visited the locality. Warm springs of small flow issue 
at several places in the valley west of the springs and suggest that 
there is also leakage at these points from deep sources. 
AGUA CALIENTE SPRINGS (SAN DIEGO 9). 

In the valley of Vallecito Creek, 35 miles southeast of Warner 
Hot Springs, are small, unimproved warm springs known as Agua 
Caliente Springs. These are near the extension of the fault through 
Warner Valley, and possibly they issue along a continuation of this 
line of structural weakness. 



HOT SPRINGS. 47 

AGUA TIBIA SPRINGS (SAN DIEGO 2). 

Near the southern base of Agua Tibia Mountain and 25 miles in a 
direct Hne north of west from Warner Hot Springs, warm water 
(agua tibia), issues along a fault zone that is parallel to the one in 
Warner Valley. The water rises with a temperature of 92°, in a 
marshy area that covers perhaps an acre. It is conducted from a 
board-curbed pool to tubs in a near-by house, for bathing and lamidry 
use. Bubbles continually rise in the pool and the water is distinctly 
sulphureted. 

Analysis of water from main spring, Agua Tibia Springs, San Diego County, Cal. 

[Analyst, M. E. Jaffa. Authority, owner of spring. Constituents are in parts per million, 

by weight.] 

Temperature 33° ('. (92° F. ) 

Properties of reaction : 

Primary salinity Dominant. 

Secondary salinity 

Tertiary salinity 

Primary alkalinity Moderate. 

Secondary alkalinity Small. 

Tertiary alkalinity Present. 

Residue: 

Soluble in water 326 

Insoluble in water 51 

Combined water and organic matter 33 

410 

Portion soluble in water: 

Sulphate (SO4) 100 

Chloride (CI) 70 

Carbonate (CO3) 36 

Chiefly sodium (Na) and potassium (K) 120 

Portion insoluble in water: 

Silica (SiOa) 21 

Calcium (Ca), magnesium (Mg), sulphate (SO4), and carbonate 

(CO3), chiefly calcium 30 

This water is essentially primar}^ saline in character, being a soft 
water of moderate mineralization. 

DELTJZ WARM SPRINGS (SAN DIEGO 1). 

In the bed of Deluz Creek, near the northwestern boundary of 
San Diego County, warm water rises, which is slightly sulphureted 
and ferruginous. The thermal character of the springs has been 
assigned to the presence of a dike of dark, aphanitic diorite, about 
6 feet thick, that cuts through the granitic country rock and crosses 



48 



SPRINGS OF CALIFORNIA. 



the creek at this point. ^ Three springs, 84° to 88° in temperature, 
here yield about 5 gallons a minute. 

The water has long been used in rock-walled pools for bathing. 
In 1888-89 a small hotel was erected and opened as a resort, but 
heavy rains in the spring of 1890 washed out the railroad between 
Deluz station and the main line at Oceanside and the property was 
abandoned as a resort for a number of years. In 1908, however, 
it was reopened as a camping and rest resort and was improved to 
some extent. 

SAN JTJAN CAPISTRANO HOT SPRmGS (ORANGE 2). 

Hot springs rise in San Juan Canyon, about 13 miles northeast 
of San Juan Capistrano. Like most of the hot springs thus far 
described, these also issue from granitic rocks and near the base 
of the steeper slopes of a portion of the coastal ranges. Two main 
springs, four minor ones, and several marshy patches are here 
situated on the western side of the canyon on slopes near the creek. 
The highest temperature recorded was 124°, and the total yield 
was estimated at about 35 gallons a minute. Other warm springs 
issue in a canyon half a mile westward. The water is slightly 
sulphureted, but, like the other hot waters of this region, it is not 
highly mineralized. 

Analysis of water from main spring, San Juan Capistrano Hot Springs, Orange County, 

Cal. 

[Analyst, Oscar Loew (1876). Authority, Wheeler report. Constituents are in parts per mfllion.] 



Temperatm-e 

Properties of reaction: 

Primary salinity 

Secondary salinity 

Tertiary salinity 

Primary alkalinity 

Secondary alkalinity 

Tertiary alkalinity 

Constituents, 

Sodium (Na) 

Potassium (K) 

Lithium (Li) 

Calcium (Ca) 

Magnesium (Mg) 

Sulphate (SO4) 

Chloride (01) 

Carbonate (CO3) 

Siliea (Si02) 



49° to 51° C. 
(120° to 123° P.) 

46 





54 

Trace. 

(?) 



By 

weight. 



Reacting 
values. 



Trace. 

Trace. 

Trace. 

Trace. 

Trace. 
64 
63 
77 



3.89 

Trace. 

Trace. 

Trace. 

Trace. 

Trace. 
1.80 
2.10 
2.55 



293 



1 Fairbanks, H. W., Geology of San Diego County: California State Mineralogist Eleventh Kept., 
p. 99, 1893. 



HOT SPRINGS. 49 

The analysis indicates a slightly mincrahzed soft water, primary- 
alkaUne saUne in character. 

These springs were formerly visited by the Indians, who built mud 
huts (temescals), for use as vapor-bath chambers. The springs are 
mentioned in the records of the Franciscan friars, who visited them 
when in charge of the mission at San Juan Capistrano. About 1885 
two or three small buildings were constructed here, and the place also 
became a resort for campers as well as for the aihng. In 1908 the 
imj^rovements consisted of a small hotel, bathhouse, and three cot- 
tages. There are ample camp grounds, and the place has been used 
mainly as a camping resort. 

CALIFORNIA HOT SPRINGS (TULARE 18). 

A number of hot springs in the Sierra issue from the granitic rocks 
that form the main part of the range. Cahfornia ,Hot Springs, 
formerly known as Deer Creek Hot Springs, are situated about 35 
miles southeast of Portersville. Four springs here issue at points 5 
to 20 yards apart along the southern bank of Deer Creek Canyon, 20 
or 30 feet above the stream bed. This group yields about 35 gallons 
a minute of water 120° to 126° in temperature. Half a mile upstream 
on the northern side of the creek, another group of one main and two 
minor springs discharges about one-third as much water at a tempera- 
ture of 105°. All of the springs are noticeably sulphureted, but they 
are not highly miner ahzed. 

Within the last few years a company of investors had made exten- 
sive improvements here. In 1908 a frame hotel and annex provided 
accommodations for about 100 people, and small cottages and tents 
erected in an ample camp ground near by have sheltered several 
hundred people at one time. Water from the upper springs, which are 
the only ones that were originally available, is j^iped to a tank, and 
thence to the baths and grounds for a cool water supply, while pipes 
from the lower group conduct the hot water about 275 yards to 
baths near the hotel. The springs of the lower group are also used 
to some extent for drinking, and are now easily reached by a foot- 
bridge and a path along the canyon side. 

The springs issue from seams in coarse-textured gray granitic 
material, which is the country rock of this region. Although no 
large fault is recognized at this locahty, other faults have been 
traced in this portion of the Sierra, and it seems probable that at 
least local fracturing has afforded escape to deep-seated water at this 
point. An analysis of what is locally known as the House Spring is 
presented herewith. 

35657°— wsp 338—15 4 



50 



SPRINGS OF CALIFORNIA. 



Analysis of water from House Spring, California Hot Springs, Tulare County, Cal. 
[Analyst and authority, Curtis and Tompkins (1911). Constituents are in parts per million.] 



Temperature 

Properties of reaction: 

Primary salinity 

Secondary salimty 

Tertiary salimty 

Primary alkalinity 

Secondary alkalinity 

Tertiary alkalinity 

Constituents, 

Sodium (Na) 

Potassium ( K) 

Lithium (Li) 

Ammonium (NH^) 

Barium (Ba) and strontium (Sr) 

Calcium (Ca) 

Magnesium (Mg) 

Iron (Fe) 

Aluminum ( AI) 

Manganese (Mn) 

Sulphate (SO4) 

Nitrate (NO3) 

Chloride (CI) 

Bromide (Br) and iodide (I) 

Carbonate (CO3) 

Metaborate (BO2) 

Arsenate ( AsO^) 

Phosphate (PO4) 

Silica (SiOz) 

Carbon dioxide (CO2) 

Hydrogen sulphide (H2S) 



51° C. 


(124° F.). 




27 














68 




5 




63 


By 


Reacting 


weight. 


values. 


60 


2.61 


.92 


.02 


.36 


.05 


.005 


.00 





.00 


1.7 


.08 


.19 


.02 


} .77 


.03 





.00 


5.5 


.12 


.51 


.00 


27 


.75 


Trace. 


Trace. 


55 


1.82 


3.0 


.08 


1.7 


.04 


Trace. 


Trace. 


54 


1.78 


211. 055 







.00 





.00 



The analytical data show that the water is soft, only slightly min- 
eralized, and primary alkaline in character. Tertiary alkalinity and 
primary salinity are noteworth}^ properties. The proportion of arsen- 
ate radicle is an unusual feature and should be taken into account in 
using this water. 

HOT SPRINGS NEAR KERNVILLE (EIIRN 11). 

The hot waters that rise at a number of places along Kern River 
suggest that the lower course of the river, as well as its upper portion, 
which is so mapped (see PI. Ill, in pocket), may foUow a fault zone. 

About 2 miles northeast of Kernville, at the base of steep slopes 
on the eastern side of the river valley, warm water seeps out at 
several places, but the main point of issuance is in a small marshy 
area in an open cove on the vaUey side. A small frame bathhouse 
has been erected here and is used locally. The temperature of the 
water is about 103°, its flow is small, and it does not taste distinctly 
mineralized. The rock at this locality is a coarse-textured granitic 
gneiss whose planes of schistosity dip steeply eastward and strike 
parallel with the valley side. 



HOT SPRINGS. 51 

NEILLS HOT SPRING (KERN 10). 

About 7 miles west of south from Kernville hot water i-ises near 
the center of Hot Spring Valley, about 1 mile east of the present 
channel of Kern Kiver. Like several other hot springs in the State, 
this was known as Agua Caliente to the Spanish settlers, and has 
been referred to under this name in a few publications. There is a 
small seepage pool 75 yards from the main spring, but the entire 
flow is now from one vent. About 40 feet of well casing was sunk 
into this spring a few years ago, and the yield was thereby materially 
increased. The water, which has a temperature of 131° and a flow 
of about 1 1 5 gallons a minute, is used for domestic purposes and 
irrigation. The ranch house is a stopping place for travelers and is 
occasionally visited by people who wish to use the baths. 

Tlie water is noticeably sulphureted, and fragments of a white 
mineral, possibly magnesite, are said to have been brought up when 
the casing was being sunk. 

The topography of Hot Spring Valley suggests that Kern River 
formerly flowed through it along the fault zone that is believed to 
exist here. 

CLEAR CREEK HOT SPRINGS (KERN 9). 

Hot water issues at three or four places among the bowlders at 
the southern edge of Kern River 200 yards below the mouth of Clear 
Creek. In 1908 the springs were seldom visited, but a few years 
earlier, during the cons traction of a power canal near by, they were 
made use of by the workmen for bathing and washing and became 
known locally as the Hobo Springs. The water is mildly sulphureted. 

DELONEGHA SPRINGS (KERN 8). 

At the western edge of Kern River, about 6 miles below the Clear 
Creek springs, is a group of three hot springs that are called after a 
prospector named Delonegha. These springs (PI. \, B) issue a few 
feet above the river surface from crevices in fractured, massive gran- 
ite. The water is distinctly sulphureted, but it does not seem to be 
otherwise notably mineralized. In 1908 there was a resort here, 
consisting of a small hotel and two bathhouses. The flow of two of 
the springs was collected in cement basins and used in the bath- 
houses, which were perched on the rocks above the river. The third 
spring issues too close to the river to be easily available. 

DEMOCRAT SPRINGS (KERN 7). 

At Democrat Springs, wliicli are 5 miles below Delonegha Springs, 
hot water issues on the southwest side of Kern River, within 150 
feet of its edge, but 50 or 75 feet above its surface. In 1908 there 
was a substantial hotel, having accommodations for 100 people, at 



52 SPRINGS OP CALIFORNIA. 

this place. One spring, having a temperature of 115° and a flow of 
about 20 gallons a minute, furnished the supply for bathing. About 
400 yards downstream from this spring, and near the hotel, a reservoir 
has been constructed around other warm springs. At a third place 
another small spring forms a drinking pool. The waters of these 
springs are sulphureted, but they do not seem to carry notable 
amounts of other mineral matter. 

With reference to the fault origin of these springs it was learned 
that although the earthquake of April 18, 1906, was not severely felt 
here, the main spring ceased flowing at that time. It was reopened 
a few months later by making a cut into the slope about 8 feet below 
the former point of issuance of the spring. 

WILLIAMS HOT SPRINGS (KERN 17). 

At the north edge of Walker Basin, about 10 miles southeast of 
the canyon of lower Kern River, on the Williams ranch, is a group 
of small thermal springs. One spring, 97° in temperature, yields 
about 8 gallons a minute of water that supphes a private bathhouse, 
and another, 150 yards eastward, with a temperature of 75°, fur- 
nishes a domestic supply. There are several cool springs of small 
flow in the same locahty, and half a mile westward other seepages 
form a meadow of several acres. The waters are distinctly sulphu- 
reted, but they are not otherwise noticeably of mineral character. 

The rock at the springs and to the north and west is granitic and is 
cut by occasional quartz ledges. One-fourth mile south of the springs 
there is a belt of granitic gneiss whose planes of schistosity, where 
noted, are nearly vertical and strike eastward. These springs are 
near the southern end of a fault that is mapped as extending down the 
canyon of North Fork of Kern River. (See PI. Ill, in pocket.) A 
probable explanation of their origin is thus offered by the fracturing 
that has taken place along this zone of displacement. 

PARADISE SPRINGS (SAN BERNARDINO 9). 

In the desert of western San Bernardino County there is an isolated 
group of thermal springs that may properly be described here. They 
are 25 miles by road north of Daggett and on the eastern slope of a 
granitic mountain. Two warm springs and a few seepages issue in 
a belt 250 yards long, on the side of a wide drainage slope that opens 
southeastward to the desert. The liighest temperature observed was 
102° and the total flow is perhaps 25 gallons a minute. 

In the early emigrant days these springs were a favorite camping 
place for travelers, and the area of green in this stretch of desert 
earned them the name of Paradise Springs. The locality is still used 
as a camping place by prospectors, and in 1908 a l|-inch pipe line 



HOT SPRINOS. 53 

extended from the springs southward and westward 2 miles to the 
Paradise Mountain gold mine. 

The water issues on slopes 500 feet above the desert floor, but 
evaporation in the region is so great that a considerable alkaline 
deposit has formed at the springs. The water rapidly corroded the 
pipe leading to the mine. 

A prospect drift exposes iron-stained graphic granite about 40 yards 
above the warmest spring, and there is a ledge of cnmipled, quartzitic 
rock near by. It seems probable tliat these dikes or ledges may act 
as dams that here bring water to the surface from moderate depths, 
at a locality where intrusive rocks have produced an abnormal tem- 
perature gradient. 

JORDAN HOT SPRINGS (TULARE 7). 

All of the thermal springs that have been thus far described issue 
from granitic rocks, are not highly mineralized, and have not formed 
notable spring deposits. In the higher parts of the Sierra, however, 
hot waters that do contain considerable amounts of dissolved solids, 
issue at several places. Jordan Hot Springs, which are situated on a 
tributary of the upper Kern River, have formed prominent deposits 
of lime carbonate, the principal one of which is shown in Plate VIII, 
B (p. 124), and the water is noticeably hard. About 14 springs issue 
in a little flat along the banks of Ninemile Creek. Four of them have 
been excavated to form bathing pools, and several others are used 
as drinking springs. The water of the latter is distinctly carbonated, 
but that of the larger springs tastes mainly of calcium or sodium. 
The principal springs that are used range in temperature from 95° 
to 123° and yield from 1 to 10 gallons a minute. 

The springs are named after the man who first blazed a trail across 
this part of the mountains, and although the locality is remote, there 
are usually parties of campers at the springs throughout the summer. 
A grove of trees and a convenient meadow make it a very good camp- 
ing ground, and an old log cabin and rude tables show that it has 
long been a campers' resort. 

In connection with the deposit of lime carbonate at Jordan Hot 
Springs may be mentioned a deposit of this material at Natural 
Bridge, about 10 miles in a direct line west of north from these 
springs, in an area of lava overlying granitic rocks. There are 
only a few pools of slightly carbonated water near Natural Bridge 
now, but springs of considerable size apparently issued there at a 
former time. On the eastern side of Kern River canyon, about 20 
miles in a direct line west of south from the Jordan springs, there is 
also an extensive deposit of lime carbonate beneath a capping of lava. 
Cool springs of small flow issue along the slopes at this place. 



54 



spRiisrGS or California. 



Jordan Hot Springs rise througli lime-cemented, granitic gravel, 
and the surrounding slopes are of granitic rocks. Three or 4 miles 
northward, however, there is some lava, and although it was not noted 
in the immediate vicinity of the Jordan springs, its presence near the 
lime carbonate deposits at Natural Bridge and in Kern River canyon 
suggests that the presence of carbonates or bicarbonates and free 
carbon dioxide in the water of Jordan Hot Springs is in some way 
related to lava rocks. 

BLANEY MEADOWS HOT SPRINGS (FRESNO 6). 

About 75 miles northward from the Jordan springs, in the canyon 
of South Fork of San Joaquin River, about a mile above the upper 
end of Blaney Meadows, three or four small springs issue on each side 
of the river and, like the Jordan springs, are used as a mountain 
camping resort. They have been dug out to form bathing pools. 
The water has a maximum temperature of about 110°, and the yield 
on each side of the river is perhaps 20 gallons a minute. The follow- 
ing is an analysis of water from the largest spring on the east side 
of the river: 

Analysis of water from main spring {east side of river) at Blaney Meadows Hot Springs, 

Fresno County, Cal. 

[Analyst and authority, F. M. Eaton (1909). Constituents are in parts per million.] 



Temperature , 

Properties of reaction: 

Primary salinity 

Secondary salinity . . . 

Tertiary salinity 

Primary alkalinity. . . 
Secondary alkalinity . 
Tertiary alkalinity . . . 



48° C. (118° F.) 

71 
24 


5 
13 



Sodium (Na)... 
Potassium (K). 
Calcium (Ca)... 
Magnesium (Mg). 
Iron ( 



^(Fe). 



Aluminum (Al). 
Sulphate (SO4).. 
Chloride (CI).... 
Carbonate (CO3) . 
Silica (Si02) 



Carbon dioxide (CO2) . 



Constituents. 



weight. 



198 
2.4 
70 
Trace. 

2.1 

58 

365 

17 



760.5 



Present. 



Reacting 
values. 



.06 

3.51 

Trace. 



1.22 
10.30 

.58 
1.61 



Present. 



The water of the springs is characterized chiefly by primary salinity 
with secondary saHnity as a subdominant property. The concen- 
tration is sufficient to render the water undesirable for many indus- 
trial uses, and its salinity is sufficient to be noticeable in taste. 



HOT SPRINGS. 



55 



The canyon is largo and rugged and is cut through massive granitic 
material. At the springs a band of gneiss is exposed, whose planes 
of schistosity dip nearly vertically to the west and strike about N. 
10° W. at a considerable angle to the canyon, which here trends 
about N. 75° E. 

LOWER SPRINGS ON SOUTH FORK OF SAN JOAQUIN RIVER (FRESNO 4). 

About 10 miles below the Blaney Meadow Springs, on the south 
side of the stream, another group of hot springs and seepages forms a 
considerable area of moist land on the slopes above the river. The 
four larger springs are used as bathing pools by campers who visit the 
place during the summer months. 

REDS MEADOWS HOT SPRINGS (MADERA 6). 

In the high Sierra east and southeast of Yosemite Valley are 
numerous meadows that are favorite summer camping places for those 
who enjoy the mountains. Reds Meadows, in the northeastern end 
of Madera County, is one of the chief of these, for it Hes at the junction 
of trails that lead east to Mono Valley, and north, south, and west to 
other portions of the mountains. On the eastern side of this meadow 
several small thermal springs issue. A bathing pool has been made at 
the largest spring, in which a temperature of 120° was recorded. The 
pool is excavated in a small deposit of lime carbonate that has formed 
at the spring. The following analysis shows the character of the 
water : 

Analysis of water from main spring, Reds Meadows Hot Springs, Madera County, Cal. 
[Analyst and authority, F. M. Eaton (1909). Constituents are in parts per million.] 



Temperature 

Properties of reaction: 

Primary salinity 

Secondary salinity 

Tertiary salinity 

Primary alkalinity 

Secondary alkalinity 

Tertiary alkalinity 

Constituents. 

Sodium (Na) 

Potassium (K) 

Calcium (Ca) 

Magnesium (Mg) 

Iron (Fe) 

Aluminum (Al) 

Sulphate (SO,) 

Chloride (01) 

Carbonate (CO3) 

Silica (SiOs) 

Carbon dioxide (CO2) 



49° C. (120° F.) 

12 


53 
35 
42 



Reacting 
values. 




56 SPRINGS OF CALIFORNIA. 

The analysis indicates water of moderate concentration in which 
salinity is relatively small, primary alkalinity, secondary alkalinity, 
and tertiary alkalinity all being prominent properties. 

The predominant rock in Reds Meadows is granitic, and the springs 
issue from such material, but on the slopes about 100 yards above 
them is a small bluff of dark, columnar lava. Along the western 
border of the meadows also there is much of this columnar rock, and 
at the Devils Post Pile, a mile northwest of the springs, columnar 
jointing is exceptionally well developed. The presence of the lava 
may account for an abnormal temperature gradient that gives rise to 
the heated water, and the high content of bicarbonates in the water 
is also worthy of note in connection with the lava. The existence of 
several carbonated springs in this locality may here be mentioned, 
though their discussion will be taken up later. 

HOT SPEINGS AT HEAD OF FISH VALLEY (FEESNO 2). 

At the head of Fish Valley and 3 or 4 miles eastward from a carbon- 
ated spring (Fresno 1, p. 239) in this valley are two warm springs and 
subsidiary seepages on the mountain side. The springs 3deld only a 
small flow, are not near a main trail, and have not been often visited. 
Their occurrence in the same region as Reds Meadows Hot Springs 
is of geologic interest, however, because thermal springs are not com- 
mon in the high Sierra. 

SLATES HOT SPRINGS (MONTEREY 4). 

In the Coast Ranges of Monterey County thermal springs of note 
issue at four places. The southernmost is at Slates Hot Springs on 
Mr. J. A. Little's ranch. The water here issues at ten principal 
points in a distance of 125 yards, halfway up the face of bluffs that 
here border the ocean. A small private bathhouse has been built 
near the easternmost spring. The waters range in temperature from 
110° to 121°, are mildly sulphureted, and the run-off streams are 
lined with abundant green algous growth. Small deposits of alum, 
gypsum, and carbonate of lime or magnesia were noted at the edge 
of one spring. The waters taste distinctly sweetish. 

About one-fourth mile northwest of the main group, on the left 
bank of Hot Creek, is another spring, 98° in temperature. This 
spring yields perhaps 5 gallons a minute and is used for laundering 
clothes. 

It is said that the location of the springs was described by an 
Indian to Mr. Thomas B. Slate, who made his way southward with 
difficulty along the steep, brushy slopes, and succeeded in findiiig only 
the warm spring beside the creek. Later, however, he came down 
the coast in a boat, found the springs on the bluff, and settled near 
them in 1868. The locality is occasionally made a camping place by 



HOT SPRINGS. 57 

deer hunters, but as it is about 17 miles by trail beyond the southern 
end of the wagon road it is not often visited. 

The formation exposed along the bluffs is of slates that have been 
described by Fairbanks ' as being probably of Jurassic age. They 
are overlain by 30 or 40 feet of gravel that is deposited on an ocean 
terrace along this portion of the coast. The heated water apparently 
emerges at the base of the gravel, though small warm flows also issue 
from the slate, close to the surf. It is said that when garden land on 
the terrace back of the springs has been irrigated for several weeks 
by a mountain stream the seepage water has so reduced the temper- 
ature of the liot springs that they are only tepid. 

DOLANS HOT SPRING (MONTEREY 5). 

A warm and mildly sulphureted sprmg exists on North Fork of 
Big Creek, about 1 h miles from the ocean and 7 miles by trail south 
of Slates Hot Springs (Monterey 4, p. 56). The water issues in a 
deep portion of the canyon, which is heavily timbered with redwoods, 
and as the place is known only locally and is not easily accessible, 
the spring has not been made use of and has been seldom visited. 

HOT SPRINGS ON NORTH FORK OF LITTLE SUR RIVER (MONTEREY 1). 

Several thermal springs rise in the bed and along the banks of 
North Fork of Little Sur River, about 2 miles above the point at 
which the stage road crosses the stream. The springs in the stream 
bed form a warm pool, and on its right bank two or three flows, havmg 
a maximum temperature of 114°, issue from crevices in the rock and 
fill a small natural basin. The springs are in a narrow, rugged section 
of the canyon, in a granitic area, and possibly rise along fractm'es 
that have been produced by local faulting. The water is mildly 
sulphureted but it is not otherwise noticeably mineralized. A con- 
siderable amount of fibrous algous growth, from white to reddish 
purple in color, is found in the stream and the adjacent pools. 

During the nineties the water was piped to a grove of redwoods 
in a flat some distance below the springs, and it was the intention 
to build a hotel and bathliouse. High water washed out the pipe 
Une, however, and in 1908 the attempt to develop the springs had 
not been renewed. 

TASSAJARA HOT SPRINGS (MONTEREY 3). 

A large amount of hot water issues at Tassajara Hot Springs, which 
are in the canyon of Arroyo Seco, in the southern part of Monterey 
County. About 17 thermal springs may be counted here, in the bed 

' Fairbanks, H. W., Stratigraphy at Slates Springs, with some further notes on the relation of the Oolden 
Gate series to the Knoxville: Am. Geologist, vol. 18, pp. 350-356, 1896. 



58 SPRINGS OP CALIFORNIA. 

of the creek and along its southern bank. They range in temperature 
from about 100° to 140° and from mere seepages to flows of 7 or 8 
gallons a minute. 

The thermal waters issue from a gneiss that is exposed along the 
creek for a distance of 200 yards or more. Above and below this 
exposure the rock is granitic and in some places contains small 
garnets. The crystalUne rocks are overlain by a series of shale, 
sandstone, and limestone whose structure in the area north of Arroyo 
Seco is well shown by the beds of massive, buff-colored sandstone 
that dip about 45° NE. A western limb of this structure was not 
seen, though it may exist in the mountains farther coastward. The 
observed dips suggest that Arroyo Seco here crosses a zone of intense 
pressure in the crystalhne rocks. 

The springs received their name from an Indian or Mexican word 
that means "the place where meat is cured by drying," and dates 
from the early days of the cattle industry. The springs have thus 
been known and used for many years, and they were early visited by 
campers, when the only access was by means of a difficult trail. 
Sevei^al years ago a well-graded wagon road was built southward from 
Jamesburg across the mountains and down into the canyon, and the 
springs are now easily reached by stage. In 1904 a stone hotel was 
built, and other improvements have been added yearly, so that in 
1909 there were ample accommodations for 75 people, though a larger 
number has been taken care of by the use of tents. Water from 
two of the largest springs has been piped to tub and plunge baths, 
and a vapor bath has been constructed over the hottest spring, which 
issues in the creek bed. 

Analyses of two of the thermal waters were made. These waters 
are noticeably sulphureted, and the analyses show them to be only 
moderately minerahzed. The water of the Arsenic Spring has a 
distinctly yellow color, which in a few other springs has been ascribed 
to alkaline sulphides in solution. 

At the north edge of the creek, a few yards above the hot springs, 
there are two cool springs in which iron is deposited. An analysis 
of the easternmost of these springs is tabulated with the hot springs. 

The identity of an early analysis ^ purporting to be of water from 
these springs seems questionable, as it does not accord with the later 
analysis. 

1 California state Mineralogist Thirteenth Rept., p. 514, 1896. 



HOT SPRINCS. 



59 



Analyses of water frovi Tassajara Hot Springs, Monterey County, Cal. 
[Analyst and authority, F. M. Eaton (1909). Constituents are in parts per million.] 



Temperature 

Properties of reaction: 

Primary salinity 

Secondary salinity. . . 

Tertiary salinity 

Primary alkalinity . . . 
Secondary alkalinity . 
Tertiary alkalinity . . 



59° C. (138° F.) 

63 



30 

7 

138 



39° C. (103° F.) 

65 





26 

9 

104 



1S° C. (64° F.) 

19 
16 



65 
(?) 



Constituents. 



By 

weight. 



Reacting 
values. 



By 
weight. 



Reacting 
values. 



By 

weight. 



Reacting 
values. 



Sodium (Na) 

Potassium (K)... 

Calcium (Ca) 

Magnesium (Mg). 

Iron(Fe) 

Aluminum (Al). . 
Sulphate (SOj)... 

Chloride (CI) 

Carbonate (CO3). 
Arsenate (AsO^). 
Silica (SiOj) 



81 
4.6 
5.3 
Trace. 

1.5 

110 
6.5 
41 



3.51 

.12 

.27 

Trace. 

.05 

2.29 
.18 
1.37 



75 
4.8 
4.0 
1.3 

2.0 

109 
5.0 
38 
aO 
116 



3.26 
.12 
.20 
.11 

.07 

2.27 
.14 

1.28 
.00 

3.84 



14 

33 

11 
0.8 
1.9 

36 

12 

61 



(?) 



355.1 



Carbon dioxide (CO2) 

Hydrogen sulphide (H2S). 



.00 
1.47 




Present. 



Present. 
(?) 



0.59 

1.64 
.87 
.03 
.21 
.75 
.32 

2.03 



Present. 



a Not detected in 1 liter of water. 
1, Lower of two main springs; 2, Arsenic Spring; 3, Iron Spring. 

The two hot springs were apparently from the same general source, 
showing only sHght differences in composition. Primary sahnity and 
primary alkalinity are the chief stable properties, but the waters are 
characterized by high tertiary alkalinity of which siHca is the chief 
component. The carbonate radicle reported is presumably calculated 
from the alkalinity determination and doubtless includes sulpliides 
and possibly sihcates. The apparent absence of arsenic in the Arsenic 
Spring is noteworthy. 

The iron spring is of markedly different character from the hot 
springs, being less than half as concentrated and having secondary 
alkalinity as the dominant property. Tertiary alkalinity is not 
reported but is probably relatively low. The spring is probably of 
essentially surface origin and is not directly related to the thermal 
waters. 

The following notes concerning algous growths in the creek below 
the hot springs are here given, as the growths are related to the sul- 
phureted character of the water. Although they are common to 
thermal sulphur springs, the relatively large volume of water at 
Tassajara Hot Springs, its comparatively slow cooling, and the 
presence of both swift currents and of quiet pools in the run-off 
stream, afford an unusually good opportunity to observe the varia- 
tion in character of the growths. 



60 SPRINGS OF CALIPORinA. 

At the main springs, where the temperature of the water was 110° 
to 140°, the material was mainly fibrous and white, green, and 
reddish-brown in color. 

About 75 yards below, at a temperature of 96°, there was a dark- 
green layer on the bottoms of pools, with a small amount of white 
material on the surface of the green. Where the current was swift- 
est, a purple-brown, furry growth, one-eighth to one-quarter inch 
thick, covered the rocks. 

At 125 yards, where the temperature was 91°, a green, leathery 
growth covered portions of the bottom, with white, feathery stream- 
ers attached to it where the current was rapid. 

At 200 yards, in a temperature of 87°, a thick, leathery growth 
coated the entire stream channel, being green and white on its upper 
surface, pale purphsh-red inside, and black on the under surface. A 
number of pale purple, feathery, and white threadlike streamers ex- 
tended from it. 

At 250 yards, in a temperature of 83°, there was a layer of green 
material in the pools and white material in the swifter water. 

At 275 yards, where the temperature was 81°, the lower limit of 
white growths was reached. Below it a dark-green moss coated the 
rocks for a distance of about 50 yards to a point where the tempera- 
ture was 78°. Below this point there was no notable growth in the 
channel. 

The material showed a tendency toward brighter colors in the hot- 
ter water and more somber ones in the cooler places. White material 
(probably due to the deposition of sulphur) was more common in the 
hottest water and in the portions of the algous growth nearest the 
bottom of the channel. Smooth, leathery growths lined the pools, 
whUe fibrous growths were formed in the swiftest currents. The 
discharge of the stream was approximately 100 gallons a minute. 
The water first rose at a point about 50 yards above the main springs. 
Above this point the stream channel was dry. 

PARAISO HOT SPRINGS (MONTEREY 2). 

Paraiso Hot Spriiigs (PI. IV, C, p. 32) are situated near the head of 
a small valley that opens eastward to Salinas Valley. Underground 
water lies at a shallow depth near the springs, beneath an area of 
several acres within which at least five mineral springs rise. The 
largest of these, which is known as the Soda Spring, has an observed 
temperature of 111° and a discharge of perha,ps 8 gallons a minute. 
About 40 yards away two small sulphur springs rise with tempera- 
tures of 88° and 102°, and 100 yards farther east there are two 
drinking springs, each of which yields perhaps one-fourth gallon a 
minute. These are known as the Iron Spring and the Arsenic Spring 
and have temperatures respectively of 68° and 65°. 



HOT SPRINGS. 



61 



The springs at this phico were known to the Cathohc mission 
fathers, who at one time Hvetl here. Their extensive modern use 
dates back more than 20 years, and their accessibihty has made 
them an objective point for automobile parties. In 1908 accommo- 
dations were provided in hotels and cottages for about 200 guests, 
while tub and plunge baths at the Soda and the Sulphur springs, and 
a swimming plunge that was also supplied by these springs, gave 
ample opportunity for use of the waters. Anal3^ses of the springs, 
luatle a number of years ago, are available and are here presented in 
the stantlard form. 



Analijses of water from Paralso Hot Springs, Monlere.ji Counti/, Cal. 
[Constituents are in parts per million.] 





1 


2 


3 


4 


5 


Temperaturo 


48''C.(n8°F.) 

81 
2 


17 
22 


48°C.(118°F.) 

85 


2 
13 
12 


46°C. (IH'F.) 

69 
10 


21 
39 


21''C. ( 


70°F.) 

51 


11 
38 
28 


21 °C. ( 


70''F.) 


Properties of reaction: 


82 


Secondary salinity 


17 
1 


Primary alkalinity 

Secondary alkalinity 

Tertiary alkalinity 






51 


Constituents. 


s 

60 

1 


1. 


s 

tuo 

1 




s 

1 

M 


to > 


60 

1 
PP 


^ . 

3 


i 


3 


St)dium (Na) 


253 
2.9 
41 
7.5 
7.3 
5.1 
493 
38 
79 


11.00 

.07 

2.04 

.62 

.26 

.56 

10.27 

1.07 

2.63 


252 
3.1 
32 


10.96 

.08 

1.60 


233 
6.4 

28 
38 

9.7 

520 
29 
94 


10.13 

.16 

1.40 

3.13 

.35 

10.83 

.82 

3.13 


234 
80 
30 

74 

12 

23 

342 

304 

Trace. 

156 


10.18 
2.05 
1.50 
6.09 

.43 

.48 

9.65 

10.13 

Trace. 

5.18 


179 

58 
23 
9.8 

3.9 

22 

387 


7.78 


Potassium (K) 


1.48 


Calcium (Ca) 


1.15 


Magnesium (Mg) ; . 


.81 


Iron ( Fe) 


463 
39 
56 


.68 

9.64 
1.10 

1.87 




Aluminum (Al) 


.14 


Sulphate (SO4) 


.46 


CMoride(Cl) 


10.92 


Carbonate (CO3) 




Arsenate ( ASO4) 






Silica (Si02) 


50 


1.66 


45 


1.49 


44 


1.46 


176 


5.84 








976.8 




909.1 




1,002.1 




1,255 




858.7 




Carbon dioxide (CO-) 


25 


1.14 


(a) 


(«) 


17 
60 


.77 
3.52 


(«) 


(a) 






Hydrogen sulphide (H2S) 























a Present. 

1. Hot Soda Spring. Analyst and authority, Winslow Anderson, 1889. 

2. Hot Soda Spring. Analyst, A. Cihi, 1871. Authority, U. S. Geol. Survey Bull. 32. 

3. Hot Sulphur Spring. Analyst and authority, Winslow Anderson, 1889. 

4. Arsenic Spring. Analyst, A. Cihi (?). Authority, advertising matter. 

5. Iron Spring No. 2. Analyst, A. Cihi (?). Authority, advertising matter. 

The Hot Soda Sprmg is primary saline in character with secondary 
alkalinity as a subdominant property. The name "Soda," given 
to this spring, is a misnomer, as the word usually applies to primary 
alkaline waters. The Hot Sulphur Spring differs from the Hot Soda 
Spring chiefly by reason of higher secondary salinity and its con- 
tent of hydrogen sulphide. The analyses of the Arsenic and Iron 
springs are of doubtful authenticity. It is of mterest that only a 
ti'ace of arsenic was found m the Ai'senic Spring and very httle iron 



62 



SPRINGS OF CALIFORNIA. 



ill the Iron Spring. Both have, primary saluiity for the principal 
property. High magnesium in proportion to calcium is indicated for 
the Hot Sulphur and Arsenic springs. 

The hUls on each side of the little vaUey at Paraiso Hot Springs con- 
sist of gravelly sandstone that dips gently away from Salinas VaUey. 
Granitic bowlders scattered along the ravines indicate that crystal- 
line rocks are exposed to the west. Although a fault is mapped 
through Salinas VaUey it is not believed that such structure has 
given rise to the Paraiso springs. It seems more probable that some 
local fold or bedrock obstruction here forces underground water to 
the surface, and that its thermal character may be due to the depth 
from which it rises, in a locality of unusually high temperature 
gradient. 

VICKERS HOT SPRINGS (VENTURA 3). 

The Coast Ranges in Ventura and Santa Barbara counties are 
composed largely of shales and sandstones of Tertiary age. At 
several places where canyons cut deeply into these sediments, ther- 
mal springs issue, and this is especially true of Matihja Canyon, in 
western Ventura County. In this canyon the westernmost point of 
note at which hot waters rise is at Vickers Hot Springs, The water 
here issues at the northeast edge of the creek from a low bank of 
stream gravel and crushed shale. A hotel and baths were con- 
structed here in 1873, but the buildings were washed away by high 
water in the spring of 1884, and when visited m 1908 the place had 
evidently been abandoned for a number of years. These are said 
to be the original MatUija Springs, and the foUowhig analysis is 
believed to be of water from this place: 

Analysis of water from main spring, Vickers Hot Springs, Ventura County, Cal. 

[Analyst, R. B. Riggs (1888). Authority, U. S. Geol. Survey Bull. 60. Constituents are in parts per 

million.] 



Properties of reaction: 

Primary salinity 

Secondary salinity 

Tertiary salinity 

Primary alkalinity 

Secondary alkalinity 

Tertiary alkalinity 

Constituents 

Sodium (Na) 

Potassium (K) 

Calcium (Ca) 

Magnesium (Mg) 

Sulphate (SO^) 

Chloride (Cl) 

Carbonate (CO3) 

Silica (Si02) 



By 
weight. 



Reacting 
values. 



546 
32 

65 
3.4 
17 

877 
58 
41 

1,639.4 



23.72 
.83 
3.24 
.28 
.35 
24.73 
1.93 
1.37 



HOT SPRINGS. 63 

This water is essontially aii iinj)iiro solution of common salt, pri- 
mary salinity being the predominant property. Tlic concentration 
is sufficient to impart a distinctly salty taste to tlio wat(U". The 
water is sulphureted, though this is not indicated by the analysis, 

STENGLEYS HOT SPRINGS (VENTURA 6). 

About one-lialf mile below Vickers Hot Springs, at the southwest 
edge of tJie creek on the property of Mr. S. G. Stingley, thermal water 
also issues. A small pool in which a temperature of 100° was re- 
corded has here been used for batliing. 

In connection with the thermal springs of this locality, tJiree small 
sulphur springs may be mentioned that have temperatures of 66°, 
76°, and 65°. They issue respectively one-fourth mile west of 
Stingleys Hot Springs, one-eighth mile northeast of them, and tliree- 
fourths mile eastward. The first mentioned is a strongly sulphu- 
reted pool at tiie base of the canyon slope and was formerly used 
as a drinking spring. The second spring issues from a sliort tunnel 
in the hiUside and yields about 2 gallons a minute of water that fur- 
nishes a domestic supply to Mr. Stingley's home. Tliis water rises 
clear but becomes milky from suspended sulphur after flowing a few 
yards. The third spring rises in a canyon on the property of Mrs. 
Gertrude A. Lyons and is piped to a small resort (see Lyons Spring, 
Ventura 6), which is described among the sulphur springs (p. 278). 

MATILIJA HOT SPRINGS (VENTURA 7). 

MatiHja Hot Springs are situated about 2J miles below Vickers Hot 
Springs and 6 miles northwest of the railroad terminus at Nordliofl. 
There has been a resort at the springs since about 1890 and improve- 
ments have been added until in 1908 there were accommodations for 
200 people. At the northern edge of the creek sulphureted water rises, 
wliich is said to have a maximum temperature of 116°. It is pumped 
to baths and to a large swimming plunge about 200 yards downstream. 
Two warm sulphur springs, at which there are cemented drinking 
basins, also issue on opposite sides of the creek near the baths. Each 
yields about 1 gallon a minute of moderately sulphureted water. 



64 



SPRINGS OF CALIFORNIA. 



The following analyses of the springs at this place have been pub- 
lished : 

Analyses of water from Maiilija Hot Springs, Ventura County, Cal, 

[Constituents are in parts per million.] 



Hot Sulphur. 



Fountain of 
Life. 



Mother Eve. 



Lithia. 



Properties of reaction: 

Primary salinity 

Secondary saUnity . . 
Tertiary salinity . . . 
Primary alkalinity. . 
Secondary alkalinity 
Tertiary alkalinity . 



52 




48 
1001 



67 



26 

7 

186 



32 


15 
53 
433 



Constituents. 



By 
weight. 



React- 
ing, 
values. 



By 
weight. 



React- 
ing, 
values. 



By 
weight. 



React- 
ing 
values. 



g React- 



Sodium (Na) 

Potassium (K) 

Calcium (Ca) 

Magnesium (Mg) 

Sulphate (SO4) 

Chloride (CI) 

Carbonate (CO3) 

Silica (Si02) 

Hydrogen sulphide (H2S) 



16 

3.5 
5.8 

12 

16 

20 

27 



8.9 
0.5 



6.09 

.44 
.04 



.25 
.45 
.67 
.90 



156 
65 
19 



4.40 

2.17 

.63 



57 
18 
78 
36 
166 
17 



3.87 

2.84 
1.48 
1.62 
1.02 
5.53 
.56 



51 

4.1 
6.9 
10 

7.3 
76 
36 



2.22 

.20 
.57 
.21 
.21 
2.53 
1.19 



100.3 



461 



191.3 



12.8 



198 



11.6 



594 



34.9 



These analyses were taken from a letterhead and recomputed on 
the assumption that hydrogen sulphide was expressed in cubic inches 
per United States gallon and other constituents in grains per United 
States gallon. The date of analysis and name of analyst are not 
given. Under such conditions not much confidence can be placed 
in the tabulated values. It is likely, however, that the general 
character of the waters is indicated at least approximately. The 
first three appear to be strongly sulphureted. Primary salinity and 
secondary alkalinity characterize the Hot Sulphur Spring. The 
Fountain of Life contains primary sahne water in which primary 
alkalinity is prominent. The water of Mother Eve Spring, though 
of higher concentration and having a less salinity, approaches that 
of the Hot Sulphur Spring in general character. The Lithia Spring 
is markedly alkaline in character, primary alkalinity being the 
dominant property. 

WHEELERS HOT SPRINGS (VENTURA 2). 

Wheelers Hot Springs are situated in the canyon of North Fork of 
Matifija Creek and are about 2^ miles north from the MatiHja 
springs. Three warm sulphureted springs rise at Wheelers and the 
place has been a resort since about 1895. The Main Hot Spring, 
102° in temperature, discharges about 35 gallons a minute into a 
swimming plunge. The two other springs, which are known as 



HOT SPRINGS. 



65 



Bucket Spring and Genoveva Spring, liave observed temperatures, 
respectively, of 62° and 75°. Each yields about one-half gallon a 
minute, of mildly sulphuretetl water, and forms a drinking pool. A 
fourth spring, also sulphureted but cool, issues at the side of a small 
storage reservoir and yields perhaps 5 gallons a minute. 

In 1908 the improvements at these springs included a hotel and 
aimex, about 35 tent cottages, a dancing floor, and bathing facilities. 
Electric Ught was supphed by a small water-power plant. 

The following analyses are of the springs at this place : 

Analyses of ivater from Wheelers Hot Springs, Ventura County, Cat. 

[Analysts, Wade and Wade (1900). Authority, advertising matter. Constituents are Ln parts per 

million.] 



Main. 



Bucket. 



Genoveva. 



Temperature 

Properties of reaction: 

Primary salinity 

Secondary salinity. . . 

Tertiary salinity 

Primary alkalinity. . . 
Secondary alkalinity. 
Tertiary alkalinity. . . 



39° C. (102° F.) 

47 



48 
5 



17° C. (62° F.) 

48 



45 
7 
6 



24° C. (7.5° F.) 

20 
30 


50 



Constituents. 



By 

weight. 



Sodium (Na) 

Potassium (K)... 

Calcium (Ca) 

Magnesium (Mg). 

Iron(Fe) 

Sulphate (SO4)... 

Chloride (Cl) 

Carbonate (CO3). 
Silica (Si02) 



333 

4.7 



4.5 



16 
245 
242 

27 



879 



Hydrogen sulphide (HjS) . 



Excess. 



Reacting 
values. 



By 
weight. 



14.49 
.12 
.34 
.37 



.34 
6.90 



.91 



328 

3.5 

12 

6.8 

Trace. 

26 

243 

243 

30 



892.3 



Present. 



Reacting 
values. 



By 

weight. 



14.26 

.09 

.58 

.56 

Trace. 

.55 

6.86 

8.09 

.99 



Present. 



Present. 



Reacting 
values. 



48 


2.07 


7.0 


.18 


144 


7.29 


20 


1.61 


259 


5.39 


6.4 


.18 


167 


5.58 


27 


.91 


678.4 





Present. 



The Main and Bucket springs are apparently much alike in com- 
position and concentration, though differing in temperature. Both 
give soft waters characterized by primary alkalinity and primary 
salinity. The Genoveva Spring differs markedly from the others, 
giving a hard water in which secondary alkalinity is the dominant 
property. The three springs are alike in that alkalinity and salinity 
are of about equal value as properties in each. Genoveva Spring is, 
however, of secondary alkalinity and salinity, while that of the others 
is primary; and the salinity of Genoveva Spring is characterized by 
the sulphate radicle, while that of the other springs is almost free from 
sulphate. 

Although the analyses of springs in Matilija Canyon do not show 
unusually high mineral contents, there are small deposits of salts at a 
few places. The most notable deposit of this kind that was observed 
35657°— wsp 338—15 5 



66 SPRINGS OF CALIFORNIA. 

is a patcli a few yards in diameter about 25 yards east of the main 
spring at Wheelers Hot Springs. At this place crystals of sulphur, 
alum, and probably Epsom salt are mingled with shale, but a hard 
conglomerate ledge is exposed near by. The waters differ widely in 
character and may differ in origin, though the differences in character 
may be accounted for on the assumption that the waters pass through 
shales and sandstones of different composition. 

The group including Vickers, Stingleys, Matilija, and Wheelers 
springs is in a region of sandstones and shales. These rocks are 
steeply inclined and have been subjected to great pressure. 

It may be that the abnormal temperatures of the waters in this 
region are due in part to chemical action of the minerals within the 
shales, but in such a region of steeply inclined beds the underground 
temperature is probably abnormally high. 

SESPE HOT SPRINGS (VENTURA 1). 

In the canyon of Sespe Creek, about 20 miles in a direct line north- 
east of Matilija Canyon, hot water issues from at least four groups of 
springs. These are situated on the bank above the creek and also in 
the gravel wash of the stream bed. The highest temperature noted 
here was 191° in a spring that issues on the steep slope, about 15 feet 
above the creek bed. The springs on the bank issue from fissures in 
partially decomposed granitic material that is here exposed beneath 
crushed shale for 300 or 400 yards. 

Although a fault has not been mapped at this locality, the San 
Andreas fault line passes about 15 miles northward, and the fractured 
condition of the rocks at the Sespe springs indicates that subsidiary 
faulting has taken place. 

The springs are best reached by road and trail from Fillmore, a 
small town on the railroad, 23 miles southward, and are visited by a 
few campers and deer hunters during the summer months. 

WARM SPRINGS IN ELIZABETH LAKE CANYON (LOS ANGELES 1). 

In Elizabeth Lake Canyon, about 25 miles east of the Sespe springs, 
there is a small group of thermal springs. They are not of high 
temperature nor notable flow, however, and are seldom visited. The 
San Andreas fault line is mapped as passing about 8 miles north of 
these springs, and its proximity suggests that the existence of the 
warm water may be due to subsidiary fracturing of the rocks where it 
issues. 

MONTECITO HOT SPRINGS (SANTA BARBARA 7). 

Montecito Hot Springs are situated about 5 miles northeast of 
Santa Barbara, in a canyon on the steep mountain side. At this 
place 11 separate springs may be counted, which issue from seams in 



HOT SPRINGS. 



67 



thick-boddeci sandstone at the upper boundary of an area of shale 
that geologically overlies the sandstone.* These springs range in 
observed temperature from 111° to 118°, and in discharge from about 
2 to 10 gallons a minute. The total yield is probably not far from 50 
gallons a minut(\ All of the springs are mildly sulphurcted and 
seem to be otherwise of similar mineral character. The following 
is an analysis of water from the main spring: 

Analysis of water from main spring, Montecito Hot Springs, Santa Barbara County, Cal. 
[Analyst and authority, Winslow Anderson (1888). Constituents are in parts per million.] 



Properties of renelion: 

Primary salinity 

Secondary salinity. . . 

Tertiary salinity 

Primary alkalinity. . . 
Secondary alkalinity . 
Tertiary alkalinity. . . 



51 
40 

'I 


n3 



Constituents. 



By 
weight. 



Reacting 
values. 



Sodium (Na) 

Potassium (K) 

Calcium (Ca) 

Magnesium (Mg).. 
Aluminum (.\1). .. 

Hydrogen (H) 

Sulphate (SO4).... 

Chloride (Cl) 

Carbonate (CO3) o. 
Arsenate (ASO4)... 
Silica (Si02) 



110 

Trace. 

30 

27 
7.9 
Trace. 
393 

18 

21 
Trace. 

20 



4.80 

Trace. 

1.52 

2.20 

.87 

Trace. 

8.18 

.51 

.70 

Trace. 

.67 



626.9 



Carbon dioxide (CO2) 

Hydrogen sulphide (H2S). 



163 
60 



7. -10 
2.55 



a If correct, this indicates an unstable condition. From the form in which the analysis was stated, how- 
ever, it appears likely that this represents alkalinity, on evaporation of the residue, soluble in water and 
may be due in part to loss of chloride on ignition. It has been so considered in stating the properties of 
reaction. 

This water belongs to the laxative class of medicinal waters, being 
characterized by sulphate salinity of primary and secondary bases. 
The tertiary alkalinity is prominent and adds to its medicinal value. 

Two small bathhouses and a hotel and cottages have been erected 
here, and the place was formerly conducted as a resort but was 
closed during 1909 and 1910. 

A portion of the water from the springs forms part of the supply of 
the Montecito Water Co. It is aerated in a screened tank and part 
of the sulphide content is thereby precipitated as sulphur and removed 
before the water enters the mains. 

SAN MARCOS HOT SPRINGS (SANTA BARBARA 2). 

San Marcos Hot Springs, which are sometimes referred to as Moun- 
tain Glen Hot Springs, are situated about 20 miles by road northwest 
of Santa Barbara, in a deep, brushy stream canyon. Warm sul- 



' See Arnold, Ralph, Geology and oil resources of the Summerland district, Santa Barbara County, 
Cal.: U. S. Geol. Survey Bull. 321, PI. I, 1907. 



68 SPEIl^GS OP CALIFOENIA. 

phureted water rises at about six places in this locality, for a distance 
of 150 yards, in the bed of the creek and along its sides. Bathing 
pools have been excavated and the place is frequently visited by 
campers, who find good camp grounds a few hundred yards below the 
springs. As at the Montecito springs, the country rock is sandstone, 
which here dips about 30° E. 

A fault which has been traced through the valley of Santa Ynez 
River passes a few miles north of these springs. Local fracturing 
in connection with this extensive movement possibly has taken place 
near the San Marcos springs and has afforded escape to deep-seated 
water. 

LAS CRUCES HOT SPRINGS (SANTA BARBARA 1). 
» 

Las Cruces Hot Springs issue on a hillside about 18 miles west of 
San Marcos Hot Springs and 4 miles northward from Gaviota rail- 
road station on the coast. Four warm springs here furnish about 
50 gallons a minute of mildly sulphureted water and in two of the 
springs inflammable gas rises. A ledge of calcareous material back 
of the largest springs probably has been formed by deposition from 
the water. In 1908 there was a bathhouse at the largest spring, 
and the place was occasionally visited by campers. 

The topographic position of the springs is worthy of note, as they 
are in a little swale on the mountain side one-half mile from and 400 
feet above the main drainage canyon of this region. Thick-bedded 
sandstone here dips about 30° SW. and strikes nearly in the direc- 
tion of steepest slope. 

NEWSOMS ARROYO GRANDE WARM SPRDTG (SAN LUIS OBISPO 9). 

Newsoms Arroyo Grande Warm Spring is situated in a small open 
canyon 2^ miles east of the town of Arroyo Grande, in San Luis 
Obispo County. The spring yields about 15 gallons a minute and 
rises in a board-curbed pool that supplies tub baths and a small 
swimming plunge. The temperature of the water is 98°. The water 
tastes moderately sulphureted, and a small amount of sulphur is 
deposited along the run-off channel. A small amount of acid salt 
also forms on the curbing of the spring, and when these salts are 
placed in the water, which is clear, a black precipitate that is prob- 
ably iron sulphide immediately forms. The constituents render the 
water unsuitable for laundry uses, but they are not objectionable for 
bathing. The following is an analysis of the water : 



HOT SPRINGS. 



69 



Anah/sis of water from Newsoins Arroyo Grande Warm Spring, San Luis Obispo 

County, Cal. 

[Analyst and authority, Winslow Anderson (1888). Constituents are in parts per million.] 



Temperature 

Properties of reaction: 

Primary salinity 

Secondary salinity . . . 

Tertiary salinity 

Primary alkalinity. . . 
Secondary alkalinity. 
Tertiary alkaUnity . . . 



38° C. (100° F.) 

34 
3 


63 
86 



Constituents. 



By 

weight. 



Reacting 
values. 



Sodium (Na) 

Potassium ( K) . . . 

Calcium (Ca) 

Magnesium (Mg). 

Iron (Fe) 

Alvmiinum (Al). . 
Sulphate (SOi).. 

Chloride (CI) 

Carbonate (CO3). 
Silica (Si02) 



62 
24 
60 
40 
33 
3 

116 
43 

216 
35 



2.70 
.61 
3.01 
3.30 
1.18 
.33 
2.41 
1.20 
7.19 
1.10 



Carbon dioxide (CO2) 

Hydrogen sulphide (H2S) . 



127 
23 



5.76 
1.38 



The water of this spring is secondary alkaline and primary saline 
in character, tertiary alkalinity being also an important characteristic. 

The property has been open to the public as a resort since 1864. 
In 1908 there were accommodations for about 30 people in a hotel 
building and small cottages. The baths have been much patronized 
on Sundays by people from Arroyo Grande, and the water has been 
carbonated and bottled by the local soda works. 

The sihceous shales that form the hills of this locality have been 
steeply uplifted and exhibit dips which show that the structure here 
is disturbed, and indicate that the spring probably rises along frac- 
tures produced at a zone of sharp change in the inclination of the 
beds. 

PECHO WARM SPRINGS (SAN LUIS OBISPO 7). 

In the canyon of Islay Creek, west of San Luis Obispo, and about 
2 miles from the coast, are two warm, disagreeably sulphureted springs 
which are known as Pecho Warm Springs. When visited in 1908 
there was a wooden trough tub and a screen of gunny sacking at the 
larger spring, while the other was used only as a drinking pool. 
Theu- observed temperatures were 95° and 72° and then- flows, respec- 
tively, about 15 gallons and 2 gallons a mmute. The larger spring 
issues at the creek edge, at the base of a 10-foot bank of crushed 
shale, the other rises about 150 yards farther downstream, and at the 
roadside 10 yards from the creek. 

The hiUs of this vicinity are composed of shales of Miocene age, 
in which the structure indicates that there has been sufficient local 
folding and crushing to account for the existence and temperature 
of the springs. 



70 



SPRINGS OF CALIFORNIA. 



The place has long been resorted to on holidays by picnic parties 
from the neighboring sheep and cattle ranches; but it has been com- 
paratively seldom visited by campers, as it is not a desirable spot for 
a vacation retreat. 

SAN LUIS HOT SPRING (SAN LUIS OBISPO 8). 

Southward from San Luis Obispo and near the ocean is a resort 
of considerable importance that utilizes the artesian flow of an unsuc- 
cessful oil well. This well was begun in the fall of 1885 and abandoned 
in March, 1887, when at a depth of 937 feet. Quantities of gas and 
warm, sulphureted water were obtained, but no oil was yielded. A 
number of years ago the water is reported to have had a tempera- 
ture of 103° and discharge of 100 gallons a minute.^ In 1908 a 
temperature of 107° was recorded. The discharge seemed to have 
materially decreased but was not measured. The following is an 
analysis of the water: 

Analysis of water from San Luis Hot Spring, San Luis Obispo County, Cal. 
[Analyst, E. W. Hilgard (1885). Constituents are in parts per million.] 



Temperature 

Properties of reaction: 

Primary salinity 

Secondary salinity 

Tertiary salinity 

Primary alkalinity 

Secondary alkalinity 

Tertiary alkalinity 

Constituents. 

Sodium (Na) 

Calcium (Ca) 

Magnesium (Mg) 

Iron (Fe) 

Manganese (Mn) 

Sulphate (SO4) 

Cliloride (Cl) 

Bromide (Br) and iodide (I) 

Sulphide (S) 

Carbonate (CO3) 

Arsenate ( ASO4) 

Silica (Si02) 

Carbon dioxide (CO2) 

Hydrogen sulphide (H2S) 



39° C. (103° F.) 

45 


32 
23 
210 



By 

weight. 



Reacting 
values. 



182 

20 

17 

49 

16 

96 

94 
1.2 
205 
171 

3.1 

27 



7.91 
1.01 
1.41 
1.74 

.57 
2.00 
2.64 

.01 
12.82 
5.69 

.07 

.91 



881.3 



120 

42 



5.44 
2.48 



This analysis is stated in per cent in the thirteenth report of the 
California State Mining Bureau and in grains per United States 
gallon in an advertising folder, but the figures are the same in both, 
except that arsenic is given as 16.06 in the report of the mining 
bureau and 0.06 in the folder. The recomputation to the foregoing 
statement was made on the assumption that in the original state- 
ments the gases were expressed in cubic inches per gallon and other 
constituents in grains per gallon, the value 0.06 being taken for 
arsenic. The most notable feature of the analysis is the large pro- 



1 California State Mineralogist Tenth Rept., p. 577, 1890. 



HOT SPRINOS. 71 

portion of sulphide radicle or free sulphur. Although the details 
of the analysis can not be considered reliable, the general primary- 
saline-alkaline character of the water and the relatively high tertiary 
alkaUnity in which sulphur is prominent are probably fairly repre- 
sented. 

Tlie well is located at the south edge of the canyon of San Luis 
Obispo Creek, 100 yards from the stream and at the border of a 
sycamore grove. A resort was early established here, and the place 
became known as Sycamore Spring, but in recent years the name 
was changed to the present title. Extensive accommodations have 
been provided, and the creek is made use of for boating. The rocks 
exposed in tliis locality consist of shales and sandstones of Miocene 
or PHocene age wliich dip mainly to the north or northeast. Anti- 
clinal or low-arched structure which would be favorable to the exist- 
ence of oil was not noted, though it may exist. 

In the summer of 1908 a well was being drilled for oil half a mile 
east of the San Luis spring, and in it a flow of gas and water similar 
to that in the early well had been obtained. 

BIMINI HOT SPRING (LOS ANGELES 11). 

In connection with San Luis Hot Spring, two hot-spring resorts 
on the outsldrts of Los Angeles may properly be mentioned here, 
as they are also unsuccessful oil wells in which flows of warm water 
were obtained. 

Bimini Hot Spring has been improved as a bathing resort, and 
also as a sanitarium, since about 1903. Tub baths and three large 
swimming plunges are here pro\4ded, and the place is extensively 
patronized by bathers. A sanitarium hotel near by is also con- 
ducted under the same management. The well is reported to yield 
100 gallons a minute of water 104° in temperature. An analysis 
of the water is tabulated beyond for comparison with that of an- 
other warm artesian well of the locality. The primary alkalinity 
of the water gives it a pecuHar soft feeling that has led to the appel- 
lation "the velvet baths." 

The well is said to have been drilled 1,750 feet deep in the sedi- 
ments of Tertiary age that make up the oil formation of tliis locality. 

RADroM STJLPHTJR SPRING (LOS ANGELES 10). ' 

About 2 miles northwest of Bimini Hot Spring a sanitarium was 
started in 1905 at another unsuccessful oil well. In 1908 the prop- 
erty changed ownership, and improvements were made, consisting 
of a pumping and heatmg plant for the water, a number of bath- 
tubs, and offices and rest rooms. The water is claimed to be notably 
radioactive. In the fall of 1908 it was placed on the local market 
as a table and medicinal water. The following is an analysis of the 
water, tabulated with an analysis of Bimini Hot Spring. 



72 



SPRINGS OF CALIFORNIA. 



Analyses of ivater from, Radium Sulphur Spring and Bimini Hot Spring, Los Angeles 

County, Cal. 

[Constituents are in parts per million.] 



Temperature 

Properties of reaction: 

Primary salinity 

Secondary salinity . . . 

Tertiary salinity 

Primary alkalinity. . . 
Secondary alkalinity . 
Tertiary alkalinity . . 



34° C. (93° F.) 



Constituents. 



By 
weight. 



Reacting 
values. 



By 
weight. 



Reacting 
values. 



Sodium (Na) 

Potassium (K)... 

Lithium (Li) 

Calcium (Ca) 

Magnesium (Mg). 

Iron (Fe) 

Sulphate (SO4)... 

Chloride (CI) 

Carbonate (CO3) . 
Arsenate (ASO4).. 
Phosphate (PO4). 
Silica (Si02) 



476 

26 

Trace. 

46 

34 

Trace. 

380 

164 

416 

Trace. 

Trace. 

21 



20.70 

.67 

Trace. 

2.29 

2.80 

Trace. 

7.91 

4.63 

13.87 

Trace. 

Trace. 

.70 



722 
21 



31.40 

.54 



6.0 
2.0 

.56 



.30 
.16 
.02 



200 
801 



5.64 
26.70 



26 



1,563 



1, 778 



Carbon dioxide (CO2) . 
Helium (He) 



Present. 
Present. 



Present. 
Present. 



1. Radium Sulphur Spring. Analyst, R. Leeman (1906?). Authority, advertising matter. 

2. Bimini Hot Spring. Analyst, L. J. Stabler. Authority, advertising matter. 

These two waters are of about equal concentration and both are 
primary in character. However, primary sahnity is the dominant 
property in the Kadium Sulphur Spring, whereas primary alkalinity 
predominates in the Bimini Hot Spring. The addition of calcium and 
magnesium sulphates to Bimini spring water would change its char- 
acter to approximately that of the Radium Sulphur Spring. 

The well at the Radium Sulphur Spring was drilled to a depth 
of 1,000 feet or more in the oil formation. A strong flow of water 
was encountered, which was with difficulty shut off, but several years 
prior to 1908 the well ceased to flow. 

PASO ROBLES HOT SPRINGS (SAN LUIS OBISPO 2). 

Thermal waters issue at a number of places near Paso Robles, in 
the upper portion of Salinas Valley. As early as 1865 a warm sul- 
phureted spring in the southern part of the town was improved for 
bathing, the spring being cemented and covered by a large masonry 
dome, and a swimming plunge being constructed. Another spring 
near by was also inclosed by masonry walls and made use of for bath- 
ing. These springs have been abandoned for several years, however, 
apparently because they have nearly or entirely ceased to flow. 

Hotel El Paso de Robles was built about 1888. It is situated in 
the western part of town, within extensive grounds that also inclose 



HOT SPRINGS. 73 

a clubhouse and a dozen cottages. A few years ago a large and very 
complete bathhouse, with modern apparatus for the therapeutic use 
of water, was built adjoining the hotel. These baths are suppHed by 
a flowing artesian well 10 inches in diameter at the top and 640 feet 
deep, that was put down behind the bathhouse and is known as the 
Main Sulphur Spring. Its temperature is reported to be 105° and 
its yield to be 2,500,000 gallons a day (1,736+ gallons a niinute)^ 
but this amount seems excessive.^ The city of Paso Robles has also 
erected a bathhouse about one-fourth mile east of Hotel El Paso de 
Robles. Its baths are supplied by a flowing well 427 feet deep, which 
yields water at a temperature of 105°. 

PASO BOBLES MFD BATH SPRINGS (SAN LUIS OBISPO 1). 

About 2^ miles north of Paso Robles there are natural warm 
springs which are used for bathing. These are locally known as the 
Mud Bath Springs. A large amount of warm water here issues about 
100 yards from the edge of SaUnas River. The springs rise mainly 
within concrete walls that were built as foundations for a bathhouse, 
but plans were changed and the springs are now of secondary im- 
portance to Paso Robles Hot Sprmgs. There is a building at the 
Mud Bath Springs, however, below whose floor there are about half 
a dozen cemented plunges, with perforated bottoms that admit the 
water. About 30 yards west of the bathhouse is a 4-inch flowing 
weU that in 1908 yielded about 8 gallons a minute of water 118° in 
temperature. The water is said to have been struck at a depth of 
140 feet. This is known as the Lithia Spring and is used for drinking, 
its water being faintly sulphureted and salty. Two natural springs 
near by are also used for drmking. One of these, the Soda Spring, 
is about 75 yards west of north from the bathhouse. When visited 
it was inclosed by a concrete curb and was equipped with a hand 
pump, but it discharged about 4 gallons a minute of warm water. 
This water has been carbonated and bottled for several years by the 
local soda works. A cool iron spring issues in a ravine 175 yards 
northwest of the bathhouse. Water from this spring was piped to 
a drinking faucet near the bathhouse, and the overflow, about 1 
gallon a minute, supphed a cattle-watering trough in the ravine. 

Southeast of the bathhouse at least half a dozen warm pools and 
seepage springs are scattered for hah a mile or more along the river 
flat that borders the present channel. Mud from one or two of these 
pools is used in the plunges at the bathhouse, and two or three of 
the flowing springs are used locally for bathing and for laundry. 
The following are analyses of several of the springs : 

' This amount would be furnished by a vertical discharge pipe 10 inches in diameter above whose top 
the water domed up approximately 10 inches. 



74 



SPEHSTGS OP CALIFORNIA. 



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HOT SPRINGS. 



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Y6 SPRINGS OF CALIFORNIA. 

The Main Sulphur Spring has a flow of primary alkaline saline 
water in which secondary alkalinity and tertiary alkalinity are minor 
properties. The three analyses of this spring indicate a gradual change 
in character toward secondary alkalinity at the expense of primary 
salinity. The Mud Bath and Sand springs are essentially primary 
sahne and are similar both in character and concentration. The 
White Sulphur Spring is distinguished from the others by a higher 
secondary salinity and large relative proportion of magnesium. 
Anderson's analyses of the Soda and Iron springs show them to yield 
primary saline waters in which secondary alkalinity is a prominent 
and primary alkaHnity a minor property. The Jaffa and Hogland 
analysis of Soda Spring represents a water of rather complex character, 
such as would be obtained by adding calcium sulphate to the water 
represented by Anderson's analysis. This may be accounted for by 
a change in the character of the water, but it is not unlikely that dif- 
ferent springs were sampled for the two analyses. 

A fault is mapped as extending southward along Salinas Valley 
nearly to Paso Robles, and two other faults have been traced in the 
hills to the west. Such broken structure may also exist at Paso Robles 
and give rise to the springs, but the warm water that issues naturally, 
and is also obtained from deep wells here, may be of artesian origin 
and be drawn from the deep alluvium. 

SANTA YSABEL SPRINGS (SAN LUIS OBISPO 3). . 

About 4 miles southeast of Paso Robles a large volume of warm 
sulphureted water rises in a ravine on the eastern side of Salinas 
Valley. In the late eighties a resort was started here, but the plans 
were not carried out, and in 1908 there was only a small private 
bathhouse at the springs. One main spring rises beneath the bath- 
house and discharges about 150 gallons a minute of water 94° in 
temperature. At the northeast corner of the bathhouse another 
warm spring of slight yield rises in a concrete basin. The water 
flows northward half a mile to a storage reservoir or artificial lake, 
and is used for irrigation. 

Small incrustations of gypsum form on stones over which the 
water flows near its source, and a small amount of acid salt is also 
deposited. The following is an analysis of water from the main 
spring. An analysis of water from the spring at the northeast corner 
of the bathhouse shows that it is practically the same as that of the 
main spring. 



HOT SPRINGS. 



77 



Aiiah/s!s of water from main spring at Santa Ysabcl Springs^, San Luis Obispo County, 

Cal. 

[Analyst and authority, \\'in,sIovv Anderson (isss). Constituents are in parts per million.] 



Temperature 

Properties of reaction: 

Primary salinit y 

Secondary salinity 

Tertiary salinity 

Primary alkalinity 

Secondary alkalinity 

Tertiary alkalinity 

Constituents 

Sodium (Na) 

Potassium ( K) 

Barium (Ba) 

Calcium (Ca) 

Magnesium (Mg) 

Iron(Fe) 

Aluminum (Al) 

Manganese (Mn) 

Sulphate (SO^ 

Chloride (CI) 

Bromide (Br) and iodide (I) 

Carbonate (CO3) 

Metaborate (BO2) 

Silica (Si02) 

Carbon dioxide (COj) 

Hydrogen sulphide (H2S) 



36° C. (96° F.) 

43 


32 
25 
37 



By 
weight. 



350 
8.1 
Trace. 
28 
46 
8.1 
6.6 
1.4 
173 
188 
Trace. 
361 

Trace. 
29 



1,199.2 



100 
31 



Reacting 
values. 



15.20 

.21 

Trace. 

1.42 

3.78 

.29 

.73 

.04 

3. 61 

5.30 

Trace. 

12.02 

Trace. 

.96 



4.54 
1.80 



This water is similar in character to that of the Main Sulphur 
Spring at Paso Robles Hot Springs. Primary salinity is the domi- 
nant property, but primary, secondary, and tertiary alkalinity are 
prominent. 

About a quarter of a mile farther up the ravine other sulphureted 
springs issue, but they are of small flow and are unimportant. 

Like the wells and springs of Paso Robles, Santa Ysabel Springs 
may be of artesian origin, but their position, 50 feet above the river 
valley, suggests that faulting has here taken place and allows the 
escape of water from a moderate depth. 



CAMETA WARM SPRING (SAN LUIS OBISPO 6). 

Cameta Warm Spring is about 30 miles southeast of Paso Robles 
and near the road toward Bakersfield. It rises in a board-curbed 
pool about 5 feet square, at the lower end of a tule patch in a creek 
channel, and yields about 3 gallons a minute, of -moderately sulphu- 
reted water 74° in temperature. Its flow is conducted a short dis- 
tance in a pipe to another pool beneath a shed, where it is used by 
the residents for bathing. 

The water rises in a region of low gravelly hills and is similar in its 
character and occurrence to Santa Ysabel Springs (San Luis Obispo 3), 
which are farther west. 



78 



SPRINGS OF CALIFORNIA. 



FRESNO HOT SPRINGS (FRESNO 9). 

Fresno Hot Springs are situated on a branch of Waltham Creek, in 
the hills of the west side of San Joaquin Valley. Several small warm 
springs issue along the west side of the canyon, from beds of shale and 
sandstone, which are the principal rocks of this region. 

The springs have long been known and were early improved as a 
resort. A new bathhouse was built in 1904 and other improvements 
have been made, so that in 1908 there were accommodations for about 
200 people. It is said that the water was formerly warmer, but during 
recent years it has become necessary to heat it for the baths. The 
springs are distinctly sulphureted, as would be expected of water ris- 
ing through shales, but they are not otherwise of notably mineralized 
character. Some crushing and faulting has possibly taken place in 
this locality and has furnished a point of escape for the springs, but 
their relatively small flow and temperatures that are not especially 
notable render them of no great geologic interest. 

MERGE Y HOT SPRINGS (FRESNO 8). 

Mercey Hot Springs rise near the extreme western edge of Fresno 
County, among the barren hills that border San Joaquin Valley. The 
main spring has been excavated to form a reservoir, is lined with con- 
crete, and is housed. It yields warm water of a peculiar "soft "taste. 

The following analysis has been published : 

Analysis of water from main spring, Mercey Hot Springs, Fresno County, Cal. 
[Analyst, Marvin Curtis. Authority, advertising matter. Constituents are in parts per million.] 



Properties of reaction: 

Primary salinity 

Secondary salinity. . . 

Tertiary salinity 

Primary alkalinity. . . 
Secondary alkalinity. 
Tertiary alkalinity. . . 




Constituents. 



Sodium (Na) 

Potassium ( K) 

Lithitim (Li) 

Barium (Ba) and strontium (Sr) . 

Calcium (Ca) 

Magnesium (Mg) 

Iron (Fe) 

Sulphate (SO4) 

Chloride (01) 

Carbonate (CO3) 

Metaborate (BO2) 

Phosphate (FOt) 

Silica (Si02) 



This water is essentially a solution of common salt with minor im- 
purities. Bubbles of gas rise in the spring and the water there has a 
faint sulphureted odor, but at the baths, 85 yards away, it has lost 
this odor. 



HOT SPRINGS. 



79 



The spring has been known since 1848, and was first used to supply 
sheep-watering troughs. Water is scarce in this region, and the 
Mercey spring is still valuable for stock watering, as well as for its 
mineral character. There was formerly a small resort here, and the 
bathing accommodations were in 1908 still patronized by people from 
the surrounding towns. For several years prior to the earthquake of 
April 18, 1906, the water was bottled for table use, but the market 
was interrupted at that time, and in 1908 had not been resumed. 

The main spring rises in an open draw at the base of low, cherty 
gravel slopes. About 100 yards eastward, at the opposite side of a 
low ridge, another small warm spring issues that is more strongly 
sulphureted, and 400 yards westward, in a ravine, is a small cool 
spring that is not noticeably mineralized, 

A dike of serpentinous gabbro 50 yards or more in thickness cuts 
across the slopes a short distance south of the springs. It may par- 
tially account for their issuance, though it is on the slope above, not 
below them. 

GILROY HOT SPRING (SANTA CLARA 9). 

Gilroy Hot Spring is situated on the side of Coyote Creek canyon, 
in the southeastern part of Santa Clara County. The spring, which 
has an observed temperature of 110° and a flow of perhaps 15 gallons 
a minute, issues in a ravine on the western side of the canyon, 200 
feet above Coyote Creek. The rocks of the area are chiefly sand- 
stones, cherts, and conglomerate. Some serpentinous and gabbroid 
rocks were noted on the slopes to the southeast, within half a mile of 
the spring, and suggest that intrusive rock may have given rise to 
the heated water at this place. The following is an analysis of water 
from the spring: 

Analysis of water from Gilroy Hot Spring, Santa Clara County, Cal. 
[Analyst and authority, Winslow Anderson (1888). Constituents are in parts per million.] 



Temperature 

Properties of reaction: 

Primary salinity 

Secondary salinity. . . 

Tertiary salinity 

Primary alkalinity. . . 
Secondary alkalinity . 
Tertiary alkalinity. . . 



Constituents. 



Sodium (Na) 

Potassium (K)... 

Calcium (Ca) 

Magnesium (Mg). 

Iron(Fe) 

Sulphate (SO4)... 

Chloride (Cl) 

Iodide (I) 

Carbonate (CO3). 
Arsenate (AsOi).. 
Silica (SiOs) 



Carbon dioxide (CO2) 

Hydrogen sulphide (H2S). 



43° C. iUO" F.) 

60 
31 


9 
62 



By 
weight. 



228 

17 
66 
43 
2.1 

185 

422 

Trace. 

46 

Trace. 

57 



1, 066. 1 



114 
61 



Reacting 
values. 



9.93 
.42 

3.30 

3.57 
.075 

3.85 
11.91 
Trace. 

1.53 
Trace. 

1.88 



5.16 
3.58 



80 SPRINGS OF CALIFORNIA. ' 

The large amount of magnesium in proportion to calcium is worthy 
of note in connection with the presence of serpentine in the locality. 
This is a primary-saline water in which secondary salinity is a 
notable property. Tertiary alkalinity is also high, adding to its 
medicinal value. 

The spring has been used as a resort since the seventies, and in 
1908 a hotel, annex, and cottages provided rooms for about 125 
guests. From a cemented and covered reservoir that has been exca- 
vated at the spring the water flows into two small plunge baths and is 
also piped to bathtubs. Besides its use for bathing, the water is 
much used for drinking and has been carbonated and bottled for a 
number of years by the soda works at Gilroy. 

WARM SPRINGS (ALAMEDA 3). 

Four warm springs that issue on the hillside bordering the lowland 
at the southeast end of San Francisco Bay have given the small 
town of Warm Springs its name. They are situated about 2 miles 
northeast of the town, within the private grounds of Mr. Joseph W. 
Stanford. One of the springs rises in the lawn adjacent to Mr. Stan- 
ford's residence. It has been inclosed to form a covered reservoir 
about 12 feet square, which furnishes part of the domestic supply 
and yields perhaps 5 gallons a minute. Two other springs rise 
beside a walk a few yards away, in open basins, from which there 
are flows of approximately 1 and 4 gallons. The larger of these two 
springs has a temperature of 86°. The fourth spring is 200 yards 
southward, in a little swale on the southern side of a knoll. It yields 
perhaps 5 gallons a minute, of water 90° in temperature, which is 
coUected in a small covered reservoir and piped to the grounds for 
domestic and garden use. 

The water of all the springs is faintly sulphureted and is considered 
to be somewhat mineralized by sodium salts. 

Sandstone, gravel, and some calcareous material form the hill slopes 
here. A fault is mapped on Plate III (in pocket) along these slopes; 
and a landslide scar some distance above the springs, and other, cooler 
springs on the higher slopes furnish local evidence that faulting has 
taken place and has probably given rise to the warm springs. At the 
time of the earthquake in April, 1906, a fifth small spring broke forth 
in the lawn near the residence and flowed for a month.' 

ROCKY POINT SPRING (MARIN 3). 

In the Coast Ranges north of San Francisco Bay are a number 
of thermal springs that form a general group in the older sediments 
of this part of the State. A warm spring that is mildly sulphureted 
rises on the beach about 6 miles northwest of Point Bonita. It is 
locally known as Rocky Point Spring, but it is exposed only at low 



HOT SPKINGS. 



81 



tide and is of littlo importanco. Pyritiforous rock that borders the 
coast here possibly furnishes the siilpliur constituent of thcs water, 
and tlie oxidation of the pyrite may account for the abnormal tem- 
perature of the spring. 

SKAGGS HOT SPRINGS (SONOMA 8). 

Along the southwestern bank of a tributary of Warm Spring Creek 
in northern Sonoma County three hot sprmgs issue in a distance 
of 75 yards. At this locality is one of the oldest resorts of the State, 
opened to the public in 1857. The region is composed of old sedi- 
mentary rocks, and the sprmgs rise from crevices in buff-colored 
material that is probably sandstone, though its appearance is tuffa- 
ceous. Eastward along the road to Geyserville, a few schistose 
ledges, serpentine bolts, and a little opalized rock, all of which are 
probably of the Franciscan formation, were noted. The sediments 
are crushed and slickensided at many places and show that the 
rocks have been much disturbed. Such crushing, which was possi- 
bly accompanied by some faultmg, may account for the escape 
of hot water at Skaggs Springs and at other places in these disturbed 
sediments. The water at Skaggs is not perceptibly sulphureted, but 
it has a distinct oily odor and taste. 

Analyses of water from main spring, Skaggs Hot Springs, Sonoma County, Cal. 
[Constituents are in parts per million.] 



Temperature 

Properties of reaction: 

Primary salinity 

Secondary salinity 

Tertiary salinity 

Primary alkalinity 

Secondary alkalinity 

Tertiary alkalinity 

Constituents 

Sodium (Na) 

Potassium (K) 

Lithium (Li) 

Barium ( Ba) 

Strontium (Sr) 

Calcium (Ca) 

Magnesium (Mg) 

Iron(re) 

Aluminum ( Al) 

Sulphate (SOj) 

Chloride (CI) 

Iodide (I) 

Carbonate (CO3) 

Metaborate (BO2) 

Silica (Si02) 

Carbon dioxide (CO2) 



54° C. (129° P.). 



5 


81 
14 
119 



By 

weight. 



Reacting 

values. 



By 

weight. 



Reacting 
values. 



879 
9.8 
Trace. 
3.0 
Trace. 
26 
61 
5.0 
Trace. 
26 
60 
1.9 
1,157 
176 
151 



38. 22 
.25 
Trace. 
.04 
Trace. 
1.30 
5.03 
.18 
Trace. 
.54 
1.68 
.015 
38.58 
4.10 
5.01 



3.8 
.19 
2.9 
.25 
15 
55 
.45 
.04 
2.4 
63 
Trace. 
1,146 
193 
120 



2, 555. 7 



2, 500. 03 



1,057 



48.00 



39.05 
.096 
.028 
.042 
.006 
.75 

4.51 
.016 
.004 
.050 

1.77 
Trace. 
38.19 

4.49 

3.98 



1. Analyst and authority, Winslow Anderson, 1888. 

2. Analyst, E. W. Hilgard. Authority, U. S. Geol. Survey Bull. 32. 

35657°— wsp 338—15 6 



82 SPRINGS OF CALIFOEnIa. 

The analyses indicate that the water is preeminently primary 
alkaline in character, resembling a solution of ordinary baking soda 
through which carbon dioxide has been passed. The presence of 
barium, strontium, lithium, and iodine,, the excess of magnesium over 
calcium, and the relatively large proportion of borates are of interest. 
The apparent lack of agreement in the tertiary alkalmity of the two 
analyses is accounted for by the omission of the carbon dioxide deter- 
mination in Hilgard's analysis. 

In 1909 water from the lowest spring was piped to baths, that from 
the central spring was piped across the creek to the laundry, and that 
from the upper spring rose in a cemented drinking basin. The 
observed temperatures were, respectively, 120°, 122°, and 135°, and 
estimated flows about 7, 5, and 3 gallons a minute. 

A fourth spring, which is cool and of small flow, formerly issued 
from the sandstone at the creek side 100 yards above the upper hot 
spring and formed a drinking pool, but in recent years it has ceased 
to be important. In 1909 a frame hotel and about a dozen cottages 
provided accommodations for 150 guests, and there is ample space 
for the erection of tents. 

HOODS HOT SPRINGS (SONOMA 1). 

Warm water issues at Hoods Hot Springs m the canyon of Dry 
Creek, near the north edge of Sonoma County. The sprmgs are of 
smaU flow and have been used only locally for bathing. They are 
probably the same that have been sometimes referred to as Fair- 
mount Hot Springs. The rocks in their vicinity, as at Skaggs, are 
chiefly crushed sediments, but garnet and glaucophane schists were 
observed at a few places eastward along the road. 

POINT ARENA HOT SPRINGS (MENDOCINO 33). 

Point Arena Hot Springs are situated in the canyon of Garcia 
Kiver, about 15 miles by road south of east from Point Arena. The 
property has been a resort since about 1895, and in 1910 a hotel, 
several cottages, and a number of tents provided accommodations 
for 100 guests. A steep trail leads from the buildings, on the canyon 
side, to the springs and the stream 200 yards away. Close to the 
northeastern side of the stream two hot springs rise in cemented 
basins about 6 feet apart and yield flows of about 1^ and 3 gallons a 
minute of mildly sulphureted water 112° and 110° in temperature. 
The water supplies tub baths in two small houses that are built over 
the stream, and a pool in the stream itself is also much used for 
bathing. The springs issue in an area of basaltic lava which extends 
for about 8 miles northwestward along Garcia River and probably 
also for some distance eastward from the springs. In 1910 graphite 
wa,s being shipped from workings about 6 miles northeast of the 



HOT SPRINGS. 83 

springs. Shales extend from the western border of the lava to the 
coast at Point Arena. ^ 

ORRS HOT SPRINGS (MENDOCINO 20). 

Orrs Hot Springs (PL IV, B, p. 32) issue along the eastern edge of 
the mabi fork of Big River, which here flows in a deep, wide canyon. 
The locaUty is a resort and stage station on the road between Uldah 
and Mendocino. A hotel and two or three cottages furnish accommo- 
dations for about 50 guests, and tents are erected during the summer 
when needed. Five springs rise near the hotel. They range in 
temperature from about 70° to 104° and have individual flows of 4 or 
5 gallons a minute. One of the springs rises in a small swimming 
plunge, and the others supply tub and plunge baths. Near one side 
of the plunge is also a drinkmg spring, 85° iii temperature and of 
seepmg flow, and at the edge of the stream, 250 yards below the 
main group, another spring that is used for drinldng issues with an 
observed temperature of 63° and a flow of about 2 gallons a minute. 

A hydrocarbon gas that was formerly used for hghting issues at the 
mam springs, but the earthquake of April 18, 1906, apparently so 
altered the points of escape of the gas that in 1909 it was no longer 
used. The water is noticeably sul})hureted, but an early analysis' 
indicates that it is only moderately minerahzed, though it has a con- 
siderable sihca content. 

The rocks of the region are of the Franciscan formation and near 
the springs consist of crushed sandstone with some chert. Serpen- 
tine and sUiceous shales were noted on the higher slopes of the 
canyon. 

The effect of the San Francisco earthquake on the springs sug- 
gests that faults subsidiary to the San Andreas rift exist in this part 
of the mountains. Local evidence of alteration in the sediments, 
however, indicates that crushing alone may be suflacient to account 
for the issuance of warm water at this point, along the bottom of 
the deep canyon. 

THE GEYSERS (SONOMA 4). 

The Geysers of Sonoma County have become widely known, both 
for their scenic features and for their scientific interest, but it is only 
proper to state that there are no true geysers, intermittently throw- 
ing out hot water, at this place. The locality is said to have been 
first brought to public notice in 1846 by a party of hunters. Its 
unusual character soon became of more than local interest, a resort 

1 Shale cliffs at the port of this settlement form a noticeable feature from the ocean, and expose beds 
that dip 40° to 65° northward. A 4-foot bed of oil sand is also exposed near the boat landing, and some 
prospecting for oil has been done near by. 

2 California State Mineralogist Tenth Rept., p. 313, IS'JO. 



84 



SPRINGS OP CALIFORNIA. 



was early opened near the springs, and a hotel and baths have been 
erected for nearly half a century. During recent years several cot- 
tages and additional bathing facilities have been constructed, so that 
in 1909 about 75 people could be comfortably taken care of. A 
narrow but well-graded road extends from Cloverdale to the hotel 




300 400 500 Feet 



Contour inierval 20 feet 



PiGUEE 1,— Map of The Geysers, Sonoma County, Cal. 

grounds. In the spring of 1910 a better road was completed from 
Healdsburg into the locality, and it was thus made easily accessible 
to automobiles. 

The main group of hot springs and vapor vents that constitute 
the so-called geysers issue on the northern side of the canyon of 
Sulphur Creek, within an area that extends about 300 yards along 



HOT SPRINGS. 85 

the canyon side and about an equal distanco north from tlio creek, 
nearly the entire active area being shown in Plate X, A (p. 140). In 
this area 12 flowing hot springs of note, 10 hot pools, and 12 vapor 
vents and areas of vaporous exhalations were counted. A cool iron 
spring at the north edge of the creek and a cool sulphureted drinking 
spring near its southern bank may be added to the number of springs 
in this area. The approximate positions of the numerous vents 
are shown on the contour map, figure 1, which is reproduced from a 
map of the property that was kindly loaned by the owner, Mr. H. A. 
PoweU. Most of the springs and vents are along a ravine that 
extends northward up the canyon side. Several cooler pools are used 
for bathing the feet or the eyes and have received such names as the 
Corn Spring and the Eye Spring. A number of others have been 
given descriptive names such as Teakettle, Washtub, and Gluepot. 
Most of the hot water is strongly acid, or sulphureted, or both. 
Crystals of native sulphur and of acid salts are deposited at many 
small vents, and efflorescent deposits of Epsom salt are formed under 
several overhanging banks. Although most of the springs issue in 
the ravine, those of perhaps largest flow issue 175 yards eastward, 
on the steep slope 50 feet above the stream. Water from these 
springs is piped across the stream and supplies the baths. Vapor 
from a large vent at the base of the slope below the springs is also 
piped across, and supplies vapor baths. The most noted vent, 
which is known as Steamboat Geyser, issues on the slope 150 yards 
north of the large springs, it being the single steam vent shown on 
the right side of the iUustration, Plate X, A. The steam is said to 
have issued originally from a small orifice, but a few years ago a 
short piece of l|-inch pipe was firmly inserted over it in a vertical 
position. In 1909 the vapor issuing through this pipe had a tem- 
perature of 205°. A steam whistle was at one time attached to the 
pipe, but its noise so disturbed the guests that it was removed. 

Analyses of a number of the waters at this locality have been 
published. These are here republished in standard form, and the 
names of the several springs, as nearly as they could be identified, are 
also placed on the map (fig. 1). 



86 



SPEINGS OF CALIFORNIA. 



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HOT SPRINGS. 



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88 SPRINGS OF CALIFORNIA. 

The waters form a remarkable series. The analyses indicate that 
all are alike in being sulphuretecl and nearly free from chloride 
radicle and in containing a relatively small proportion of primary 
bases. The bathing water and Indian and Eye springs are similar 
in many respects. Secondary alkalinity is the most prominent 
property in the three, but in the bathing water the alkalinity is due to 
borates, in the Indian Spring to carbonates, and in the Eye Spring 
to silicates, if the analyses are correct and complete. In all the 
other waters tertiary salinity is specially noteworthy, being an unusual 
characteristic of natural waters. Excess of magnesium over calcium 
is also of interest. 

The rocks of this region consist of crushed and altered sandstones 
and shales, with cherts, schists, and associated serpentine, which form 
a part of the Franciscan formation. In the localities where the 
vapors and hot waters issue the sandstone is greatly altered, being 
changed to a clinker-like siliceous material. Serpentine is exposed 
along the canyon side between Steamboat Geyser and the main 
ravine. The presence of the serpentine at this place is of interest 
from the fact that two magnesia springs issue near what appears 
to be its southern border. Water from one of these springs is car- 
bonated and bottled as Geyser Water. 

At several places on the north side of Sulphur Creek, both above 
and below The Geysers, there are areas where the rock has been 
bleached and decomposed by solfataric action, and at a few of them 
hot water and vapor still issue. Indian Spring, of which an analysis 
has been given, is a warm pool about three-quarters of a mile west 
of the hotel. 

LITTLE GEYSERS (SONOMA 5). 

About 4 miles above The Geysers, at a locality known as Little 
Geysers, vapor and hot water issue in notable amounts. At this 
place there is an area of perhaps one-quarter of a square mile on open 
slopes within which the rock has been bleached and altered, but the 
surface activity of heated water is now mainly confined to an area 
about 200 yards in diameter. Three small hot springs, seven hot 
pools, and four vapor vents were counted here. A cabin has been 
built near by and a small bathhouse at one of the springs has been 
used by miners and, in summer, by campers. About 250 yards below 
the cabin the largest hot spring that was noted in this locahty rises 
at the creek edge and is used as a drinking pool. It yields about 5 
gallons a minute of faintly sulphureted water, 160° in temperature. 

About 1 mile southward from Little Geysers is the Socrates quick- 
silver mine. The relation of the quicksilver deposits to hot springs 
and to areas of lava has been mentioned by Becker,^ with special ref- 

1 Becker, G. F., Geology of the quicksilver deposits of the Pacific slope: U. S. Geol. Survey Mon. 13, 
p. 404, 1888. 



HOT SPRINGS. 89 

crence to areas northward and eastward from Little Geysers, but his 
conclusions are probably just as applicable to the area in the canyon 
of Sulphur Creek. He considers that the cinnabar in the ELnoxville, 
yEtna, and Sulphur Bank localities has been deposited by the action 
of the hot waters. 

ANDERSON SPRINGS (LAKE 65). 

Anderson Springs are situated about 5 miles northwest of Middle- 
town, along a branch of Putah Creek. A resort has been conducted 
at this place for many years, and in 1910 a hotel and several cottages 
provided accommodations for 150 guests. 

Nine springs that differ in character of water emerge at rather 
widely separated points on the property, but are reached by paths 
that form pleasant walks along the wooded canyon. The Cold 
Sidphiu- Spring, which is the farthest downstream, issues from 
schistose material at the creek edge 300 yards east of the hotel. It 
has been protected by a cement basin and yields a small flow of 
cool, clear, rather strongly sulphureted water used for drinking. 
About 400 yards by trail eastward and southward from the hotel, in a 
little gulch on the side of a ravine, is the Sour Sprmg, which yields a 
slight flow of water that tastes of alum. The sprmg is perennial, 
but it seems to be supplied by surface water that becomes mineralized 
by seeping through crushed sedimentary material. Across the creek 
and about 100 yards northeast of the hotel, in a rock-waUed pool at 
the creek edge, is Father Joseph Spring, which yields mildly sulphu- 
reted water that is pleasant for drmking and is considered to be a gentle 
laxative. Belmer Spring is 675 yards west of the hotel and beneath 
a gravel bank at the north side of the creek. The water rises in a 
pool a few feet in diameter and also in a barrel sunk near by. It is 
much used for drinking, but it tastes disagreeably strong of sulphides. 
The other five springs form a group about 325 yards farther upstream, 
where they issue from banks of greatly altered sedimentary rock. 
The Hot Spring, which is the principal one, rises in a barrel that forms 
a drmkhig pool. The water is thence piped to a small reservoir and 
a bathhouse near by. This water is mildly sulphureted and when 
cooled somewhat it is a palatable drinking water. Near it are two 
short tunnels that also yield warm water of similar character, and a 
few yards away vapor vents are utihzed in small steam-bath cabinets. 
The other two springs are a few yards westward, across the creek. 
One forms a pool about 3 feet across, wliich is normally covered with 
an iridescent film, possibly of iron, and is known as the Iron Spring. 
Efflorescent salts — probably sulphates of aluminum and of iron — 
crystallize on the adjacent banks. The other sprmg is about 60 yards 
away, in a branch ravine. It yields clear water that tastes strongly 
of alum, and the banks near by are also usually coated with alum. 



90 



SPEIlSrGS OF CALirORISriA. 



The waters of these last two springs have been only shghtly used and 
are not fit for drinking, as they are too astringent. 

The following tables give the approximate temperatures and flows 
of the springs and the results of analyses that were made a number 
of years ago : 

Approximate temperature andfloiu of Anderson Springs, Lake County, Cal. 



Spring. 



Cold Sulphur Spring 

Sour Spring 

Father Joseph Spring 

Belmer Spring 

Hot Spring 

Tunnel south of Hot Spring 
Tunnel west of Hot Spring . 

Unused pool 

Unused spring 



Tempera- 
ture. 



T. 



63 
63 
64 
75 
146 
100 
97 
93 
97 



Flow 
(gallons a 
minute.) 



Analyses of water from Anderson Springs, Lake County, Cal. 
[Authority, Winslow Anderson. Constituents are in parts per million.] 



Teraperature 

Properties of reaction: 

Primary salinity 

Secondary salinity . . . 

Tertiary salinity 

Primary alkalinity. . . 
Secondary alkalinity . 
Tertiary alkalinity. . . 



17° C. (63° F.) 

20 
18 



62 
411 



23° C.(74° F.) 

19 
36 




45 
504 



18°C.(64° F.) 

7 
42 
51 


61 



51°C.(124°F.) 

19 

79 





2 

220 



63° C.(146° F.) 

20 
30 


50 
355 



Constituents. 



By 

weight. 



React- 
ing 
values. 



weight. 



React- 
ing 
values. 



By 
weight. 



React- 
ing 
values. 



By 
weight. 



React- 
ing 
values, 



By 

weight. 



React- 
ing 
values. 



Sodium (Na) 

Potassium (K) 

Lithium (Li) 

Ammonium (NH^) . 

Calcium (Ca) 

Magnesium (Mg) . . . 

Iron (Fe) 

Aluminum (Al) 

Manganese (Mn) . . . 

Sulphate (SO4) 

Chloride (CI) 

Carbonate (CO.3) . . . 
Metaborate ( B 62) . . 
Arsenate ( ASO4) . . . 
Phosphate (PO4)... 
Silica (Si02) 



Ill 

Trace. 



4.81 
Trace. 



54 
Trace. 
Trace. 



2.36 

Trace. 

Trace. 



185 
117 
3.9 



9.25 

9.60 

.14 



132 
43 
1.0 
Trace. 



6.61 
3.50 
.035 
Trace. 



413 
11 
446 



8.60 
.32 

14.87 



Trace. 

""42" 



Trace. 
"1^39" 



317 

6.7 
172 
Trace. 
Trace. 



6.60 
.19 

5.72 
Trace. 
Trace. 



3.2 
6.7 
Trace. 
.7 
10 
17 
6.7 
19 
1.1 
220 



0.14 

.17 

Trace. 

.04 

.52 

1.39 
.24 

2.13 
.04 

4.57 
.02 



21 
9.0 
Trace. 



0.92 

.23 

Trace. 



35 
11 

Trace. 



1.52 

.27 

Trace. 



Trace. 



Trace. 



56 
25 
9.8 
.8 
14 
283 
1.9 
27 
Trace. 



2.79 

2.09 

.35 

.09 

.52 

5.88 

.05 

.91 

Trace. 



72 



2.39 



1.6 

72 



.05 
2.40 



92 

30 

1.1 

Trace. 

5.2 

206 

4.6 
139 

Trace. 
Trace. 
1.7 
113 



4.59 

2.48 

.04 

Trace. 

.19 

4.28 

.13 

4.64 

Trace. 

Trace. 

.05 

3.75 



1,328.9 



797.7 



521.1 



638.6 



Carbon dioxide (CO2) 

Hydrogen sulphide (H2S) 



2,072 
28 



94.20 
1.62 



1,273 
62 



57.80 
2.67 



8.1 



598 
22 



27.20 
1.30 



1. Sulphur Spring. Analyst, Winslow Anderson (1888). 

2. Belmer Spring. Analyst, Winslow Anderson (1889). 

3. Sour Spring. Analyst, G. E. Colby (1889). 

4. Iron Spring. Analyst, G. E. Colby (1889). 

5. Hot Spring. Analyst, G. E. Colby (1889). 



HOT SPRINGS. 91 

Tho analyses iiidicati^ that tlio waters of tlio Sulpliiir, Belmor, and 
Hot springs do not difi'or greatly in chemical character. All three are 
secondary waters in which salinity and alkaluiity are about equally 
promuient, but the difFerences m concentration and tho unusually 
largo content of manganese hi the Hot Sprhig are of hiterest. The 
Iron Sprmg is characterized by somewhat lower concentration and a 
higher content of iron than the other three, and it differs from them 
m properties of reaction chiefly by reason of a greater jiroportion of 
sulphate and a smaller proportion of carbonate. The Sour Spriag is 
characterized by a still greater proportion of sidphate and absence of 
carbonate, and, as is common m waters havmg tertiary salinity, con- 
tams notably large amounts of u*on and alumuium. Considermg the 
sprmgs as a group, it appears that the differences in character 
anay have been acquh^ed in the passage of water of the Sour Spring 
type through calcareous shale and magnesian limestone, the Iron 
Sprmg representing a phase in which the water encountered but 
little limestone. 

East of Anderson Springs lava covers the surface, but near the Cold 
Sulphur Spring a schist is exposed which forms the surface rock west- 
ward, and through which the several sprmgs issue. At the group 
near the Hot Spring it has been altered by solfataric action to the 
characteristic white, siliceous material that is so plentiful at The 
Geysers, a few miles to the northwest. In a tunnel-like chamber 
excavated in it near the Hot Spring, ciuantities of Epsom salt form a 
thick efflorescence on the walls, and on the surface slopes outside a 
yellow coatmg is deposited that has been collected and used as a 
catarrh powder. An analysis of a sample of it that was made by 
Anderson ^ showed that it consists largely of calcium carbonate, 
with the sulphates of calcium, magnesium, and sodium, and the car- 
bonates of the latter two bases in smaller amounts. 

This small area at Anderson Springs that show^s the effects of sol- 
fataric action is of especial geologic mterest m its resemblance to the 
areas at Little Geysers (Sonoma 5, p. 88), and The Geysers (Sonoma 
4, p. 83), which are respectively about 4 and 7 miles in a dhect line 
northwestward across the St. Helena Range. 

CASTLE HOT SPRINGS (LAKE 54). 

Castle Hot Springs are situated about 1 mile by steep trail on the 
mountam side west of Anderson Sprmgs (Lake 55, p. 89). Basins 
or small reservou's have been excavated and cemented at two hot 
spi-ings that issue a few yards apart in a ravine that is tributary to 
Putah Creek. The observed temperatures in these basins were 160° 
and 164°. Their combined flow — about 8 gallons a mmute — could 
probably be increased by developmg two or three near-by seepages 

1 Anderson, Winslow, Mineral springs and health resorts of California, p. 88, 1892. 



92 SPRINGS OF CALIFOENIA. 

of hot water. The water is mildly sulphureted but is otherwise only 
slightly mineralized, as is shown by the following partial analysis: 

Analysis of water from Castle Hot Springs, Lake County, Cal. 

[Analyst, Curtis and Tompkins (1909 ?). Authority, advertising matter. Constituents are in parts per 

million.] 
Properties of reaction : 

Primary salinity Small. 

Secondary salinity Small. 

Tertiary salinity 

Primary alkalinity Moderate. 

Secondary alkalinity Dominant. 

Tertiary alkalinity (?) 

Residue: 

Combined water 19 

Soluble in water 152 

Insoluble in water 175 

346 

Portion soluble in water: 

Sulphate (SO4) 24 

Chloride (CI) 6 

Carbonate (CO3) 60 

Sodium (Na) and potassium (K), cHefly sodium 62 

Portion insoluble in water : 

Silica (SiOj) 113 

Calcium (Ca), magnesium (Mg), and carbona,te (CO3), cMefly 

calcium 62 

The analysis indicates a secondary alkaline, primary alkaline water 
in which silica is present in relatively large proportion. 

The position of these hot springs high on the mountain side is 
worthy of note, and it is also of geologic interest with respect to the 
hot springs at Anderson Springs, a mile eastward and 800 feet lower, 
and at The Geysers, a few miles northwestward across the range and 
1,000 feet lower. In another ravine, about 700 yards by path from 
Castle Hot Springs, but perhaps half that distance in a direct line and 
100 feet lower two groups of cool sulphur springs seep from the banks. 
The rock near the hot springs consists of hard schistose material that 
is not greatly decomposed, but near the cool springs it has been 
altered, apparently by solfataric action, and is impregnated with 
sulphur and sulphate salts. 

The property was formerly known as Mills Hot Springs and was at 
one time conducted as a small resort, the hot water being used for 
bathing and the water of the cool sulphur springs for drinking. In 
the summer of 1910 the property had recently changed ownership 
and was being reimproved as a resort. A hotel, a bathhouse con- 
taining a svmnming plunge, and a dancing pavilion were being erected, 
and several tent cottages provided accommodations for a few guests. 



U. S. GEOLOGICAL SURVEY 



WATER-SUPPLY PAPER 333 PLATE VI 




A. HOUGH SPRINGS, LAKE COUNTY. 




B. HARBIN SPRINGS, LAKE COUNTY. 




a HOWARD SPRINGS, LAKE COUNTY. 



HOT SPRINGS. 



93 



The buildings are about one-fourth mile from the hot springs, on a 
ridge that commands a good view of the valley of Putah Creek and 
the mountains eastward. 



GORDON HOT SPRING (LAKE 46). 

Gordon Hot Spring rises on the eastern side of Cobb Valley Creek, 
near the head of a small meadow. A number of years ago this spring 
was used to some extent for bathing, but in 1909 the small bathhouse 
had been removed and the spring was unused. It yielded about five 
gallons a minute of water at a temperature of 92°. The water has a 
slightly oily taste, like that at Skaggs Hot Springs. (See p. 81.) 

The following is an early analysis of the water: 

Analysis of ivaterfrom Gordon Hot Spring, Lake County, Cal. 
[Analyst and authority, Winslow Anderson (1SS8). Constituents are in parts per million.] 



Temperature 

Properties of reaction: 

Primary salinity 

Secondary salinity , 

Tertiary salinity 

Primary alkalinity 

Secondary alkalinity , 

Tertiary alkalinity 

Constituents 

Sodium (Na) 

Potassium ( K) 

Calcium (Ca) 

Magnesium (Mg) 

Aluminum (Al) 

Sulphate (80^) 

Chloride (CI) 

Carbonate (CO3) 

Silica (SiOs) 

Carbon dioxide (CO2) 



38° C. (100° F.) 

38 
32 


30 
5 



By 
weight. 



Reacting 
values. 



2U 

7.0 
195 

68 

32 
532 
216 
226 

39 



9.18 
.18 
9.72 
5.60 
3.57 
11.08 
6.08 
7.52 
1.29 



1,526.0 



Excess. 



The analysis indicates a primary and secondaiy saline water in 
which secondary alkalinity is prominent. Tertiary alkalinity is not 
fully reported but is probably high. The large proportion of alu- 
minum shown by the analysis is unusual for such a water and is 
probably in error. 

The rocks of this locality are sediments that are overlain by lava 
and by siliceous tuff in which opaline silica is common. A ledge of 
quartzitic schist that contains considerable amounts of albite and 
chlorite is exposed 50 yards northeast of the spring. 

HARBIN SPRINGS (LAKE 66). 

Harbin Springs (PI. VI, B) are in southern Lake County, about 
3i miles north of Middletown. Three springs, known as the Arsenic, 
Iron, and Sulphur springs, rise close together in a ravine on the western 



94 



SPRINGS OF CALIFOEISriA. 



side of a branch, of Putah Creek, and yield water at temperatures of 
90°, 116°, and 120°, at a rate of 1, h, and 8^ gallons a minute, respec- 
tively. The property has been a resort for many years and the water 
of the Iron and Sulphur springs is used in tub and plunge baths. 
Buildings have been erected from time to time, so that in 1909 accom- 
modations for about 200 people were provided by a hotel, a three- 
story rooming house, 8 or 10 cottages, and a dozen tent houses. A 
large building containing a gymnasium and dancing floor provides 
means for entertainment. The waters of four springs at this place 
have been analyzed. One of the springs, which was called the Mag- 
nesia Spring, was originally of slight flow and is no longer important, 
but the following analyses show the characters of the three others: 

Analyses of xoater from Harbin Springs, Lalce County, Cal. 
[Analyst and authority, Winslow Anderson. Constituents are in parts per million.] 



Temperature 

Properties of reaction: 

Primary salinity 

Secondary salinity . . . 

Tertiary saUnity 

Primary alkalinity. . . 
Secondary alkalinity . 
Tertiary alkalinity . . . 



50° C. (122° F.) 

47 
22 


31 
34 



47° C. (116° F.) 

40 



28 
32 
38 



32° C. (90° F.) 

28. 


12 
60 
24 



Constituents. 



weight. 



Reacting 
values. 



By 

weight. 



Reacting 
values. 



weight. 



Reacting 
values. 



Sodium (Na). 

Potassium (K) 

Lithium (Li) 

Calcium (Ca) 

Magnesium (Mg).. 

Lron(Fe) 

Aluminum ( Al) . . . 
Manganese (Mn) . . 
Sulphate (SO4).... 

Chloride (CI) 

Carbonate (CO3) . . 
Metaborate (BO2). 
Arsenate (As04)«. 
Silica (Si02) 



252 
17 



10.98 
.43 



192 
17 



8.35 
.43 



136 
72 
11 
15 



6.79 

5.90 

.39 

1.66 



14 
42 
16 
6.6 



.71 

3.43 

.56 

.73 



476 
239 
234 



9.92 
6.76 
7.80 



144 

78 

248 



3.00 
2.19 

8.27 



.017 
1.56 



.79 



121 

40 

Trace. 



7.7 

20 

Trace. 

63 

110 

345 

Trace. 

3.1 

33 



5.28 
1.02 

Trace. 

2.28 

7.11 

.27 

2.21 

Trace. 
1.32 
3.09 

11.49 

Trace. 
.067 
1.09 



1,499.8 



874.8 



Carbon dioxide (CO2) 

Hydrogen sulphide (H2S) . 



36 



1.65 
4.56 



53 
Trace. 



2.41 
Trace. 



o Reported as "arsenious salts" and recalculated from sodium arsenate. 

1. Sulphur Spring. Analyst and authority, Winslow Anderson (1888). 

2. Iron Spring. Analyst and authority, Winslow Anderson (1889). 

3. Arsenic Spring. Analyst and authority, Winslow Anderson (1889). 

The water of the Sulphur Spring appears from the analysis to 
be of mixed type and rather high concentration; its most note- 
worthy peculiarity is the content of hydrogen sulphide. The 
Iron and Arsenic springs are similar in concentration and character, 
both possessing marked primary alkalinity as well as primary salinity 
and secondary alkalinity. The relatively high proportion of magne- 
siimi is of interest and, in connection with the relative amounts of 



HOT SPRINGS. 95 

other radicles, it indicates probable contact with magnesium-rich 
rocks. As its name implies, the x4.raenic Spring contains an exception- 
ally large proportion of arsenic and its content of aluminum is also 
uncommon for an alkaline water. All the springs contain iron in 
unusual proportion. 

Shale that dips at steep angles is exposed on the hillsides near 
Harbin Springs, but about 25 yards above the springs a belt of 
amphibolite schist appears. Its observed thickness is about 25 yards 
and its lower side apparently crosses the ravine very near the point 
at which the sprmgs emerge. As the high tilting of the sediments 
is the only other geologic feature noticed that might account for the 
springs at this place, it appears probable that the schist at least 
furnishes a point of escape for deep waters, and it possibly also aids 
in giving the water its abnormal temperature. The conditions pre- 
sented by this rock cutting through the sediments just above the 
springs may be similar to those at Mercey Hot Springs, in Fresno 
County. (Seep. 78.) 

HOWARD SPRINGS (LAKE 51). 

About 9 miles southwest of the town of Lower Lake a group of 
mineral springs (PL VI, C, p. 92), several of which are notably warm, 
issue in a line about 50 yards long at the base of a slope that borders 
the south side of a dramage course. A number of seepages have been 
dug out and cemented to form drinking basins, so that about 26 
improved springs may be counted, although the group is said to 
include 42 sprmgs. Of the 8 springs that are of chief importance 5 
are used for drinking and have been named Bohemia, Neptune, 
Lithia, and Magnesia Twins. They have observed temperatures, 
respectively, of 66°, 70°, 73°, 71°, and 100°. Wlien the witer visited 
it in 1909, Bohemia Spring discharged about 1 gallon a minute, 
while the other three rose in basins from which there was no appreci- 
able overflow. The largest three springs are used mainly for bathing. 
Of these, the Hot Soda or Hot Sulphur Spring has a temperature of 
110° and discharges approximately 125 gallons a minute into a plunge 
bath. Excelsior or Borax Spring, with a temperature of 95° and a 
flow of perhaps 5 gallons a minute, also supplies a plunge bath. 
Water from Eureka Spring is piped to tub baths, its temperature 
being 107° and its yield perhaps 2 gallons a minute. The available 
analyses of several of the springs are here given in form convenient 
for comparison. ^ 

1 The analyses of Lithia Spring and Bohemia Spring, published in advertising matter, have not been 
reproduced, as they appear to be incorrectly stated. 



96 



SPRINGS OP CALIPOPtNIA. 



Analyses of ivater from Howard Springs, Lake County, Cal. 
[Constituents are in parts per million.] 



Temperature 

Properties of reaction: 

Primary salinity 

Secondary salinity. . 

Tertiary salinity 

Primary alkalinity. . 
Secondary alkalinity 
Tertiary alkaliaity. . 



43°C.(110°F.) 

27 


28 
45 
100 



24°C.(75°F.) 

77 



18 

5 

152 



29°C.(85T.) 

34 





Trace. 

66 

142 



39°C. (102°r.) 

24 


26 
SO 
61 



16°C.(60°F.) 

16 


22 
62 
141 



Constituents. 



By 

weight. 



React- 
ing 
values, 



By 

weight. 



React- 
ing 
values. 



By 
weight. 



React- 
ing 
values. 



By 

weight. 



React- 
ing 
values. 



By 
weight. 



React- 
ing 
values. 



Sodium (Na) 

Potassium (K). . 

Lithium (Li) 

Calcium (Ca) 

Magnesium (Mg) 

Iron(Fe) 

Aluminum (Al). 
Chloride (CI).... 
Carbonate (CO3) 
Silica (SiOz) 



Carbon dioxide (CO2). 



628 

230 

0.3 

25 

313 

60 

0.9 

580 

1,317 

58 



27.29 

5.88 
.04 

1.25 
25.72 

2.30 

.10 

16.36 

43.82 

1.92 



846 
10 
1.0 

27 

8.0 

10 

0.3 

1,069 

280 

224 



36.78 

.26 

.14 

1.33 

.65 

.36 

.03 

30.18 

9.32 

7.43 



200 

132 
0.2 

136 

208 
2.4 
1.7 

427 

721 

143 



8.70 

3.38 

.03 

6.79 

17.11 

.09 

.19 

12.04 

23.97 

4.74 



556 

177 
0.1 
46 

324 
6.1 
1.4 

481 
1,331 

158 



24.17 

4.53 

.01 

2.30 

26.63 

.22 

.16 

13.58 

44.28 

5.24 



240 
115 



10.44 
2.94 



151 

169 
1.0 
1.2 

202 
875 
119 



7.53 

13.90 

.04 

.13 

5.70 

29.11 

3.95 



3,212.2 



2,475.3 



1,971.3 



3,080.6 



1,873.2 



1,277 



58.00 1,140 



51.80 1,021 



45.27 



1. Em-eka Spring. Analyst, W. T. Wenzell. Authority, Winslow Anderson. 

2. Excelsior Spring. Analyst, W. T. Wenzell. Authority, 12th Cal. 

3. Neptune SpriQg. Analyst, W. T. Wenzell. Authority, Winslow Anderson. 

4. Magnesia Twins Spring. Analyst, W. T. Wenzell. Authority, Winslow Anderson. 

5. Soda spring, not identrfied. Analyst, W. T. Wenzell. Authority, 12th Cal. 

The analyses show that the waters of these springs are ahke in 
many respects, the chief points of difference being the small pro- 
portion of secondary bases and alkaUnity in the Excelsior and the 
small proportion of primary alkahnity in the Neptune. The high 
concentration, high tertiary alkahnity, and magnesic character of all 
the springs and the iron content of the Eureka are specially note- 
worthy. The absence of any report on the sulphate radicle casts 
doubt on the trustworthiness of the analyses. 

All the springs issue in an area of serpentine within the shales and 
sandstones that form the principal part of the hills in this locality. 

The springs have been improved as a resort since about 1880. In 
1909, besides a main hotel building and the baths, the improvements 
included a large annex to the hotel and four or five small cottages. 

Waters from the lithia, Bohemia, and Eureka springs were formerly 
bottled for table use, but their sale was discontinued several years 
prior to 1909. 

SEIGLEB, SPRINGS (LAKE 49). 

Seigler Springs are situated about 2 miles northwest of Howard 
Springs, across a ridge and in the drainage basin of another 
creek. Like Howard Springs, they have been used as a resort for 
many years. The group includes 13 that in 1909 were improved to 
some extent. Of this number 6 are of small flows, range in tempera- 



HOT SPRINGS. 



97 



ture from 68° to 107°, and are used in a minor way for drinking. 
Two others, known as the Magnesia and Hot Geyser springs, also 
used for drinking, yiekl perhaps one-eighth and 2 gallons of water a 
minute, at temperatures, respectively, of 64° and 98°. The Hot 
Geyser, which has been in part developed by sinldng a 3-inch casing 
90 feet deep, is said to have received its name because prior to the 
earthquake of April 18, 1906, it spouted about once a day, but since 
the earthquake this action has nearly or entirely ceased. Its water 
has a slight oily taste and odor, such as was noted at Skaggs and at 
Gordon springs. A ninth spring, laiown as the Arsenic Spring, yields 
water 96° in temperature, at a rate of about 5 gallons a minute, and 
is used both for drinking and bathing, and two other springs with 
somewhat warmer water and about the same flow supply Hot Iron 
baths. The two hottest springs, with temperatures of 119° and 126° 
and flows of perhaps 4 and 13 gallons a minute, respectively, issue at 
the edge of Seigler Creek and supply tub baths near by. 

The Seigler Springs, like the Howard Springs, issue from serpentine 
and are situated on a gentle slope that borders the southern side of 
the creek, but they are scattered over a larger area, about 250 yards 
across. Near the southeast border of the spring area is a prominent 
ledge of siliceous rock. The higher slopes are covered with lava, and 
downstream, below the springs, the usual crushed sediments appear. 

The available analyses of springs at this place are here presented: 

Analyses of water from Seigler Springs, Lake County, Cal. 
[Analyst, not given. Authority, advertising matter. Constituents are in parts per mUlion.] 



Temperature 

Properties of reaction: 

Primary salinity 

Secondary salinity . . . 

Tertiary salinity 

Primary alkalinity. . . 
Secondary alkalinity. 
Tertiary alkalinity. . . 



wccee-F.) 

33 

7 


60 
24 



22°C. (72°F.) 

49 


11 
40 
27 



32°C.(90°F.) 

50 


12 
38 
27 



38°C.(100°F.) 

49 


16 
35 
30 



37°C.(98°F.) 

51 


12 
37 
54 



Constituents. 



weight. 



Sodium (Na) 

Potassium (K)... 

Calcium (Ca) 

Magne.sium (Mg). 

Iron (Fe) 

Sulphate (SO^)... 

Chloride (Cl) 

Carbonate (CO3). 
SUica(Si02) 



127 

26 

42 

126 

9.1 

0.4 

266 

342 

124 



1,062.5 



Carbon dioxide (CO2). 



Ee- 
acting 
values. 



By 

weight. 



5.50 

.66 

2.09 

10.33 

.33 

.01 

7.50 

11.40 

4.11 



208 

52 

22 

71 
2.3 

27 
282 
266 
141 



1,071.3 



Re- 
acting 
values. 



By 

weight. 



9.05 
1.33 
1.10 

5.84 
.08 
.56 



230 

80 

26 

74 

1.4 

1.7 

344 

292 

156 



1, 205. 1 



Re- 
acting 
values. 



By 
weight. 



10.00 
2.05 
1.30 
6.08 
.05 
.04 
9.70 
9.74 
5.17 



272 

51 

22 

75 

4. 

20 

336 

319 

180 



1,279.4 



Re- 
acting 

values. 



By 
weight. 



11.81 
1.30 
1.10 
6.17 
.16 
.42 
9.48 
10.64 
5.97 



221 

52 

21 

64 

1.3 

3.7 

312 

253 

182 



1,110.0 



69 



Re- 
acting 
values. 



9.61 
1.33 
1.05 
5.26 
.05 



8.42 
6.04 



3.16 



1. Soda Spring. 

2. Magnesia Spring. 

3. Arsenic Spring. 

4. Iron Spring No. 3. 

5. Geyser Spring. 

35657°— wsp 338—15- 



98 



SPRINGS OF CALIFORNIA. 



The names of the springs are apparently misleading as to their 
mineral content, for the analyses show that the waters of the Mag- 
nesia, Arsenic, Iron No. 3, and Geyser springs are practically identical 
in character, and the water of the Soda Spring differs from them 
chiefly in its greater proportion of magnesium. 

A frame hotel, a large stone dining room, and four or five cottages 
in 1909 provided accommodations for about 150 guests. In addition 
to the mineral water tub and plunge baths, bathing facilities were 
provided by a dam across the creek, which made a swimming pool, 

HOT SPRINGS AT SULPHUR BANK (LAKE 38). 

.Near the southeast edge of the eastern arm of Clear Lake there are 
abandoned sulphur and quicksilver workings. During the period of 
mining, water at a temperature of 176° was encountered at the fifth 
level in what is known as the Hermann shaft.^ In January, 1910, 
the water stood about 15 feet below the surface in this shaft, and 
its observed temperature was 120°. Many bubbles were rising and 
the water had the odor of sulphureted hydrogen. About 200 yards 
east of north from the shaft, in an area of decomposed basalt where 
sulphur was formerly obtained, water stands in several pools and 
issues from numerous vents. The highest temperature observed 
in these pools was 118° in a small one over which there was a bathing 
hut. Two analyses of water from this locality, made a number of 
years ago, are reproduced, as they probably show the general char- 
acter of the water that still rises. 

Analyses of water from mine shafts at Sulphur Bank, Lake County, Cal. 

[Analyst, W. H. Melville (1884?). Authority, U. S. Geol. Survey Water-Supply Paper 237. Constituents 

are in parts per mUlion.] 



Hermann shaft. 



Parrott shaft. 



Properties of reaction: 

Primary salinity 

Secondary salinity . . . 

Tertiary salinity 

Primary alkaliaity. . . 
Secondary alkalinity . 
Tertiary alkalinity . . . 





50 
2 
136 



Constituents. 



By 
weight. 



Reacting 
values. 



By 
weight. 



values. 



Sodium (Na) 

Potassium (K) 

Ammonium (NH4). 

Calcium (Ca) 

Magnesium (Mg) . . . 

Iron (Fe) 

Sulphate (SO4) 

Chloride (Cl) 

Carbonate (CO3) . . . 
Metaborate (BO2)- - 
Silica (Si02) 



1,706 

25 

24 

21 

5.5 



74.19 

.65 

.13 

1.07 

.45 



17 

693 

1,140 

800 

37 



.35 

19.54 

38.00 

18.60 

1.23 



1,320 
39 
1.1 
20 
1.6 
.5 
466 
667 
220 
1,023 
42 



57.39 

1.01 

.06 

1.02 

.1-3 

.02 

9.70 

18.79 

7.32 

23.80 

1.39 



3.2 



Carbon dioxide (CO2) 

Hydrogen sulphide (H2S) . 



262 
4.6 



11.82 
.27 



79.60 
.04 



1 Becker, G. F., Geology of the quicksilver deposits of the Pacific slope: U. S. Geol. Survey Men. 13, 
p. 259, 1888. 



HOT SPRINGS. 99 

The analyses indicate tliat the waters are stronc^ly primary alkaline 
m character. They differ chiefly in tertiary alkalinity and the relative 
prominence of salinity and alkalinity. The difference would be 
practically eliminated if sulpluiric acid or sulphate of iron or other 
heavy metals were added to the water of the Hermann shaft. 

The slopes near the Sulphur Bank mines are composed mainly of 
sediments that have been considored Lower Cretaceous in age, but 
wliere the waters rise the rock is basalt that has been extensively 
altered by solfataric action. 

In his description of the quicksilver deposits at this place Becker ^ has 
remarked on the apparent absence of any quicksilver minerals in 
solution and has spoken of the presence of boron in the water. The 
boron and the thermal character of the water are especially note- 
worthy in connection with the presence of the lava at this locality. 
A small cold carbonated spring that issues from the gravel near the 
lake edge, one-fourth mile west of the Hermann shaft, may also be 
mentioned in connection with the lava at Sulphur Bank. 

Warm carbonated waters emerge at a number of places along the 
western border of Clear Lake, notably at Soda Bay and at John 
Behr's ranch, and are described with the carbonated springs (pp. 191- 
193), but are here mentioned as they are also thermal and rise from 
volcanic rocks. 

WILBUR HOT SPRINGS (COLUSA 9). 

In the valley of Sulphur Creek, in southwestern Colusa County — 
a region where considerable minmg for quicksilver has been carried 
on — are several groups of springs that yield hot sulphureted water. 
The lowest, easternmost group is at Wilbur Hot Sprmgs, whicn has 
been a resort for more than 40 years. It was originally known as 
Simmons Hot Springs, and the resort to which the name Wilbur Hot 
Springs was applied was 4 miles to the northwest, near the Elgin 
quicksilver mine; a number of years ago, however, after the hotel at 
the latter place burned, the Simmons property was purchased by the 
owners of Wilbur Hot Sprmgs and the upper place was abandoned. 
In 1908 the present Wilbur Hot Springs (PI. IV, D, p. 32) again changed 
ownership, and most of the buildings, which were in poor condition, 
were removed and new cottages built. 

The hot springs issue along the borders of Sulphur Creek, for a 
distance of about one-half mile on the Wilbur property, but are 
mainly in a barren, saline area that borders the west side of the creek 
from 75 to 200 yards west of the hotel. The position and approxi- 
mate extent of this area are shown at the left in Plate IV, D. The 
principal springs have been numbered by the owners, beginning at 
the western border of the property, on the assumption that eventually 

1 Op. cit., pp. 259, 260. A detailed description of the geology at Sulphur Bank is given on pp. 251-257. 



100 SPRINGS OP CALIFORNIA. 

there will be 30 developed springs, though only 12 have been of 
importance. Several of the group yield cold water. 

Spring No. 1 , a hot sulphur spring, issues mainly in a pool a few 
feet west of the Wilbur property, on land that belongs to the Man- 
zanita Mining Co., but warm water also seeps out several yards east 
of the main pool. This pool has been used occasionally as a foot bath, 
but in 1910 the adjacent seepages had not been developed. 

The Hot Black Sulphur Spring (No. 10) is a few hundred yards east 
of No. 1 and about 500 yards west of the Wilbur Hotel. Its water 
issues at the southeast edge of the creek, and when visited formed a 
pool that was covered by a tent and used as a foot bath. 

The Main Springs (No. 22) are about 200 yards west of the hotel, at 
the upper edge of the barren area along the creek. Two concrete 
basins or small reservoirs, a few feet apart, are built around the 
springs, which yield a flow of hot, strongly sulphureted, and salty water 
at a measured rate of 30,000 gallons a day (21 gallons a minute). 
The water is clear and its color is distinctly yellow, like that of the 
water from Lower Blue Lick Sprmgs, Ky., whose color has been 
assigned by Palmer ^ to alkalme sulphides in solution. The more 
strongly mmeralized waters of the Wilbur springs probably contain 
alkaline sulphides in solution in medicinal amounts, but this character 
was not shown in the form in which the analyses were reported. The 
water is piped to coolmg tanks and thence to tubs in an adjacent 
bathhouse, opposite the hotel. A thin crust of white, apparently 
amorphous sulphur rapidly collects on the surface of the water in the 
cooling tanks. On being disturbed it settles as a sludge, of which a 
considerable quantity has been used as a salve. 

A few feet north of the Main Sprmgs is a smaller one, over which 
a men's mud-bath house has been built. A continual flow of water 
in the mud bath is thus directly obtained. A women's mud-bath house 
has been constructed in the same way, over another spring 30 or 
40 yards eastward. Near the northeast corner of the men's mud- 
bath house there is a shallow pool, about 4 feet in diameter, called 
the Chromatic Spring, for material that changes color from day to 
day and is probably of algous (vegetable) nature usually coats its 
bottom. On one morning it was bright green m the central part 
of the bottom and reddish purple over the marginal third. On 
the following morning the coating had a uniform dark-olive tint. 
The water is said to be sometimes as black as ink and to contain a 
black substance (probably iron sulphide) that gradually settles. At 
other times the pool is clear and contains no noticeable growth. In 
connection with the water of this spring, a red water may be men- 
tioned, that during hot dry weather collects in a few small depressions 

1 Matson, G. C, Water resources of the bluegrass region, Kentucky, with a chapter on the quality 
of the waters by Chase Palmer: U. S. Geol. Survey Water-Supply Paper 233, p. 209, 1909. 



HOT SPRINGS. 



101 



ill tlie rock surface of the barren area. It is usually crusted with 
salts and is a saturated solution. On evaporation it forms crystals 
that have been examined microscopically by R. C. Wells and are con- 
sidered to be probably potassium sulphate and sodium chloride, the 
former predominating. The red coloring matter easily passes through 
filter paper and is rendered only slightly less .distinct by boiling. It 
may be a mmute vegetable organism, but a bottled sample of the 
water retained its color after standing four years. 

The Catarrh and Complexion Spring (No. 20) issues on the south 
side of the creek, about 120 yards east of the Main Sprmgs. Like 
the other springs its water is sulphureted and strongly salty, its 
chemical character being shown by the analysis on page 102. It 
has been used as a tonic drinking water, as a douche, and as a 
shampoo, being considered to be efficacious in removing dandruff. 
Three small sprmgs are in basins a few feet apart in a spring house 
southeastward, across the creek from the hotel. The western one 
(No. 24), which is called the Cold Magnesia Spring, is the pleasantest 
for drinking and is the one most patronized. The central one (No. 
26), which is also a magnesia spring, tastes more noticeably of 
magnesia. No. 28 is a cold sulphur spring. The Cold Black Sul- 
phur Spring (No. 30) is on the south side of the creek, beyond the 
stable and about 125 yards east of the hotel. It has been protected 
by a board curbing and cover and jdelds a moderately sulphureted 
but palatable water. Jackson Sulphur Spring seeps from the road 
bank across the creek from No. 30. Its water tastes sulphureted and 
magnesic, and has been used slightly for drinking, but it is locally 
believed that its use tends to produce headache. Eastward, down- 
stream from the Jackson Spring, there are several other cool, sul- 
phureted seepages, but in 1910 these had not been developed. 

The followmg tables give the approximate temperatures and flows 
of the principal sprmgs, and analyses of those that had been chem- 
ically examined prior to August, 1910: 

Approximate tem-perature and flow of principal springs at Wilbur Hot Springs, Colusa 

County, Cal. 



Spring No. 1 , a hot sulphur spring 

Spring No. 10, Hot Black Sulphur Spring 49 120 5' 

Spring No. 22, Main Springs 60 140 21 

Men's mud-bath spring 43 110 1 

Women's mud-bath spring 43 110 1 

Chromatic Spring 49 120 1 

Spring No. 20, Catarrh and Complexion Spring 47 116 5 

Sp'ing No. 24, Cold Magnesia Spring. 

Spring No. 26, a magnesia spring 

Spring No. 28, a cold hlte sulphur spring 

Spring No. 30, Cold Black Sulphur Spring 

Jackson Sulphur Spring 



Temperature. 


"C. 


°F. 


43 


110 


49 


120 


60 


140 


43 


110 


43 


110 


49 


120 


47 


116 


16 


60 


16 


60 


18 


64 


21 


69 


18 


65 



Flow 
(gallons 

a 
minute). 



102 



SPRINGS OF CALIFORNIA. 



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T-i CQ CO -^ »0 CD 



HOT SPRINGS. 103 

Springs 10, 20, and 22 (analyses 1, 2, and 3) yield waters practically 
identical in character; that is, they give primary saline waters in 
which primary alkalinity is rather prominent. The lithium, ammo- 
nium, nitrate, hroniide, iodide, and metaborate determinations in the 
analyses are of interest. The waters of springs 24, 28, and 30 (anal- 
yses 4, 5, and G) are characterized by primary salinity and second- 
ary alkalinity of about equal prominence. The relatively high pro- 
portion* of magnesium in these three cold springs is noteworthy. 

The barren area along Sulphur Creek apparently consists of a con- 
glomerate containing fragments of sandstone, and several of the 
springs issue from fissures in it. The main country rock of the local- 
ity is, however, serpentine. This material extends eastward nearly a 
mile to an area of shales and sandstones along Bear Valley, and west- 
ward about three-fourths of a mile from the Wilbur Hotel to an 
area of shales along Sulphur Creek. A belt of sandstone 100 yards 
Avide is apparently included in the serpentine between springs 10 and 
22, and small patches of sandstone that also appear to be inclusions 
in the serpentine were noted. The locality is one in wliich intense 
geologic action has taken place and there has been much secondary 
mineralization of the rocks. ^ The thermal character of the water is 
evidently closely related to the geologic structure, and its mineral 
character to the close association of serpentine (a magnesia-bearmg 
rock), with marine sediments which probably furnish the saline and 
sulphur constituents. 

JONES HOT SPRINGS (COLUSA 11). 

Jones Hot Springs are near Sulphur Creek and about three-fourths 
mile west of Wilbur Hot Springs (Colusa 9, p. 99). The resort that has 
been built up at the place in recent years is patronized during the 
summer by many people who use the water. Accommodations for 
guests are supphed by a hotel and several cottages and by camping 
grounds near by. 

The principal yield is from a well that was bored near the creek at 
a place where gas formerly issued. Hot, sulphureted, salty water 
was obtained, which rises under considerable artesian pressure in a 
concrete tower to a height of about 12 feet, whence it flows to a 
bathhouse near the hotel. Gas intermittently rises with the water and 
causes it to spurt above the top of the tower. This characteristic 
has led to the well being named Fountain of Life. 

The well is near the western border of a serpentine area; but its 
water probably comes mainly from sedimentary rocks, for siliceous 
shales are exposed across the creek, a short distance north of it, in 
the workings of a quicksilver mine. 

1 Fairbanks, H. W., Some remarkable hot springs and associated mineral deposits in Colusa Coimty, 
Cal.: Science, vol. 23, pp. 120-121, 1894. 



104 SPRINGS OF CALIFORNIA. 

HOT SPRINGS ON MANZANITA MINING PROPERTY (COLUSA 10). 

Between Jones and Wilbur hot springs, on a strip of land that is 
part of the Manzanita mining property, similar hot sulphur springs 
issue in at least three places. The spring farthest east, which has been 
mentioned in connection with Wilbur spring No. 1, forms a pool a few 
feet in diameter that yields perhaps 1 gallon a minute of sulphureted, 
salty water, 110° in temperature. It is clear and distinctly yellow in 
color, like that of the Main Springs at Wilbur's, and hke the latter 
shows a deposit of sulphur on its surface. In 1910 the spring was 
protected by a roof and was occasionally used as a foot bath. An- 
other spring farther upstream, on the northwest edge of the creek, 
was protected by a tent and used for bathing; the third spring is 
about 100 yards northeast of Jones's Fountain of Life spring. The 
third spring, which is between the creek and the wagon road, issued 
from a wooden curbing near an old, unused bathhouse and yielded 
perhaps IJ gallons a minute of sulphureted salty water, 142° in tem- 
perature. All three of these springs issue in an area of serpentine, 
but the saline content of their water is probably derived from the 
altered sediments that outcrop a short distance to the west along the 
upper course of Sulphur Creek. 

BLANCKS HOT SPRINGS (COLUSA 12). 

A number of years ago there was a small hot-spring resort, known 
as Blancks Hot Springs, about half a mile west of Jones Hot Springs 
(Colusa 11, p. 103). When the Wideawake mining shaft was sunk 
near by, Blancks Hot Springs ceased flowing and the resort was 
closed, but of late years, since the shaft has been abandoned and has 
become partly fiUed up, the springs have resumed their flow. In 
1910 there were two springs in a small ravine behind a former room- 
ing house. One of them yielded perhaps 2 gallons a minute from a 
vertical pipe that extended a foot above the surface, and the other, 
a few yards away, discharged about an equal amount through a pipe 
that extended to a tub in a small bathhouse near by. The water is 
sulphureted and salty, and, like that of several other springs in the 
locaHty, it is clear yellow in color. It issues from sandstone that is 
well exposed and dips almost vertically to the northwest. 

HOT SPRINGS AT ELGIN MINE (COLUSA 7). 

The Elgin quicksilver mine is situated on the western side of 
Sulphur Creek, on steep slopes 400 to 500 feet above the stream. 
Much work has been done in these mines and occasional rich pockets 
of cmnabar have been found, but the tunnels have been very difii- 
cult to work in because of the high temperature, the hot water, the 
sulphureted and ammoniacal vapors, which afi^ect the eyes as well as 
the respiration, and the acid salts, which quickly destroy clothing. 
In addition to the cinnabar considerable amounts of sulphur were 



HOT SPEINGS. 



105 



formerly obtained from higher slopes near the quicksilver tunnels, 
and a few hundred dollars worth of gold is said to have been obtained 
incidentally from one quicksilver working.^ 

Hot springs, from which water was formerly piped down the slope 
to a bathhouse at the original Wilbur Hot Springs resort, still yield 
a flow of several gallons a minute on the steep slope, and a short dis- 
tance away a flow of about 10 gallons a minute at 140° tempera- 
ture issues from the Judge Moore tunnel, which extends 200 feet into 
the hill. The follomng analysis, made a number of years ago, prob- 
ably is of water from the formerly used spring at this locality: 

Anahjsis of water from original Wilbur Hot Springs, Colusa County, Cal. 
[Analyst and authority, Winslow Anderson (1S89). Constituents are in parts per million.] 



Properties of reaction: 

Primary salinity 

Secondary salinity . . . 

Tertiary salinity .' 

Primary alkalinity. . . 
Secondary alkalinity. 
Tertiary alkalinity. . . 



Constituents. 



By 

weight. 



Reacting 

values. 



Sodium (Na) 

Potassium { K) . . 

Calcium (Ca) 

Magnesium (Mg). 

L-on(Fe) 

Aluminum (Al).. 
Sulphate (SCO.- - 

Chloride (Cl) 

Iodide (I) 

Carbonate (CO3). 
SUica(Si02) 



304 

7.4 
162 
104 

26 

36 
910 
209 

10 
182 
119 



13.23 

.19 

8.07 

8.58 

.94 

3.95 

18.95 

5.90 

.08 

6.08 

3.95 



2, 0G9. 4 



Hydrogen sulphide (H2S) . 



The analysis indicates that the water is primary and secondary 
saline in character. Iron, aluminum, siUca, and hydrogen sulpliide 
are notably prominent. The water is evidently not nearly so strongly 
minerahzed as that of the Main Springs at Wilbur Hot Springs. 

The spring known as the Big Pool is about 250 yards farther north- 
west along the hillside and at the front of a large mining cut. Soft 
mud surrounds and nearly fills this pool, which is about 15 feet across 
and 2 feet deep. When visited in 1910 gas rising in the pool 
caused vigorous ebullition in two places, and water 153° in tempera- 
ture overflowed at a rate of perhaps 15 gallons a minute. The water 
tasted strongly of hydrogen sulphide, ammonia, and salt. During 
the operation of the mine this water was used in a mill near by, but it 
rapidly corroded the machinery. 

Two carbonate formations in this locaUty are of geologic interest 
in connection with the springs. One, a hard, white material that 
incloses fragments of shale, is best exposed on slopes below the Judge 



1 Fairbanks, H. W., loc. eit. 



106 SPRINGS OF CALIFOENrA. 

Moore tunnel, and forms a prominent ledge from which bowlders have 
rolled down to the lower slopes. A specimen of the material was 
examined quahtatively by K,. C. Wells, who found that it consisted 
mainly of calcium and magnesium carbonates, with only small 
amounts of silica and water. It is not dolomite but is proba- 
bly similar in composition to the material from Philhps Soda 
Springs (Napa 8), of which a quantitative analysis is given (p. 162). 
It differs chiefly from tlie latter in being much harder and in contain- 
ing very little water. About one-half mile upstream from the Elgin 
mine a ledge of onyx marble crosses the creek. This material is of 
interest in connection with the hot springs farther downstream, as 
it is considered to be a hot-spring formation. The deposit has not 
been worked commercially, but a few specimens, of a brown color, 
have been made into paper weights and other small articles. 

The hot springs near the Elgin mine issue from sediments in which 
secondary minerals, especially cinnabar, sulphur, and gypsum, have 
formed. In several places the rock has been greatly altered by 
solfataric action, and in these places a sihceous sinter has been pro- 
duced which resembles that at The Geysers (Sonoma 4, p. 83). The 
rock formation is also apparently similar to that at The Geysers, 
as it consists of sediments with associated serpentine. Although 
notable amounts of efflorescent salts were not observed near the 
springs of the Elgin mine, and there are no vapor vents, in several 
other respects these hot springs are intermediate in character between 
those farther down the creek and The Geysers of Sonoma County. 

■ The water of Sulphur Creek is warm and salty in the neighbor- 
hood of the hot springs, and between the Elgin mine and Jones 
Hot Springs it contains great numbers of slender, jointed creatures 
that attain a length of about 2 inches. These organisms, which 
are locally called "duck worms," were also found in two or tliree 
small, warm, salty streams a few miles to the northeast; but they 
were not observed in a fresh-water stream that enters Sulphur Creek 
between Jones Hot Springs and the Elgin mine nor do they thrive 
below Jones Hot Springs, where the water is possibly rendered 
uninhabitable to them by taiUngs from the quicksilver mill opposite 
these springs. They were not observed elsewhere in the State. Their 
presence is noteworthy, as it appears to be closely connected with 
the chemical character of the water. 

CRABTREE SPRINGS (LAKE 5). 

Crabtree Springs are situated in a narrow part of the canyon of 
Rices Fork of Eel River, 14 miles by road northwest of Bartlett 
Springs (Lake 9, p. 200). The springs were filed on by Mr, Crabtree 
about 1875 and a road was built to the property, but high water soon 
washed out the greater part of this road, and for many years the 
springs have been accessible only by trail. In 1910 the property 
changed ownership, however, and the road was rebuilt. 



iiOT sriuNus. 107 

The principal spring emerges at the northeast edge of the stream 
in a natural rock basin at the foot of a small cliff, and yields perhaps 
10 gallons a minute of water 105° in temperature. Considerable 
gas, probably carbon dioxide, issues with the water. The latter is 
mildly carbonated and is distinctly mineralized by salts of soda and 
probably also of iron. The pool formed by this spring has long been 
used for bathing and the water is locally considered efficacious in 
the treatment of skin and blood diseases. About 20 yards southeast- 
wartl, upstream from the main spring, a smaller flow of similar water 
issues from a seam in the rock at the creek edge, while 100 yards 
upstream from the main spring there were, in 1910, three vigorously 
bubbling, iron-stained pools that contained water 6S° to 75° in tem- 
perature. An area several yards in diameter in the creek channel 
near by was also vigorously bubbling. It is said that there was 
formerly a carbonated spring of considerable flow at this spot, but 
that it was buried by a landslide a number of years ago and during 
recent years has been in evidence chiefly by the large amount of gas 
that escapes. 

The springs are probably submerged during periods of high water, 
but during the summer the stream carries only a fewyniner's inches, 
and in some years may become dry for a short time. 

The springs issue from siliceous rock similar in character to that at 
-^tna Springs in Napa County (p. 156) and at other localities in the 
State where quicksilver has been mined. A number of years ago 
two tunnels were driven into the canyon side a short distance below 
the Crabtree Springs, in search of quicksilver. The rock contains 
noticeable amomits of cinnabar, but this mineral was not found in 
paying quantity. The siliceous rock is closely associated with ser- 
pentine, which is exposed for a few yards between the two groups of 
springs on the northeast bank, and for a short distance on the south- 
west side of the stream. There is also a cliff of the siliceous rock 
opposite the main spring; but the principal material on the south- 
west side of the canyon near the springs, and on the slopes both 
above them and upstream from them, consists of altered shale and 
sandstone. The serpentine of this locality appears to be the north- 
ward continuation of a narrow belt that extends, with some branch- 
ing or perhaps widening of the main zone, northward from Bartlett 
Springs to this place, where it appears to be less than 100 yards wide. 
The close relation of several carbonated springs to this belt of ser- 
pentine is later referred to in the description of Royal Spring (Lake 
6, p. 202). Like these others, the presence of Crabtree Springs and the 
temperatures of their waters seem to be closely related to the serpen- 
tine and the sihceous rock. The association of serpentine, sihceous 
rock, and altered sediments with warm carbonated water at this place 
is apparently similar to their association farther southward, at -^tna 
Springs (Napa 2, p. 156). 



108 



SPRINGS OF CALIFOENIA. 



CALISTOGA HOT SPRINGS (NAPA 4). 

At Calistoga/ near the head of Napa Valley, are several hot springs 
at which during the seventies there was a large resort. The hotel 
burned in the late seventies or early eighties, however, and since that 
time the springs have not been of more than local importance. In 
1910 the caretaker of the property had provided two bathhouses of two 
tubs each, half a dozen small cottages on the place were rented, and a 
few campers had pitched their tents near by. Hand pumps supplied 
hot water directly to the tubs, and cool water was piped from a tank. 

Four main springs rise at the base of a knoll of buff-colored tuffa- 
ceous material at the northern border of the meadow land, and a few 
pools and seepages of hot water appear in the meadow itself. The 
observed temperatures of the principal springs range from 126° to 
173° and their flows from about one-fourth gallon to 5 gallons a 
minute. The hottest spring, which yields about 1 gallon a minute, 
appears to be the most strongly mineralized, though its mineraliza- 
tion is only slightly perceptible to the taste. Algse probably give it 
the slight flavor that has caused it to be called a chicken-soup spring. 

At Calistoga Hotel, about 400 yards west from the springs, a dug 
well supplies warm water for tub baths and a swimming plunge. 
Warm water is also obtained in several other wells near by and there 
is one strongly flowing artesian well. The following analyses show 
that the waters are primary saline in character: 

Analyses of tvater from Calistoga Hot Springs, Napa County, Cal. 
[Analyst and authority, Winslow Anderson (1888). Constituents are in parts per million.] 



Temperature 

Properties of reaction: 

Primary salinity 

Secondary salinity 

Tertiary salinity 

Primary alkalinity 

Secondary alkalmity . . . 
Tertiary alkalinity 

Constituents. 

Sodium (Na) , 

Potassium (K) , 

Calcium (Ca) 

Magnesium (Mg) 

Iron(Fe) 

Aluminum ( Al) 

Manganese (Mn) 

Sulphate (SO4) 

Chloride (01) 

Iodide (I) 

Carbonate (CO3) 

SUica(Si02) 

Hydrogen sulphide (H2S). . . 



41° C. (106° F.) 

85 



10 
5 

33 



50° C. (122° F.) 

90 
2 





43 



35° C. (95° F.) 

75 
10 


15 
41 



By 
weight. 



Reacting 
values. 



weight. 



Reacting 
values. 



By 
weight. 



Reacting 
values. 



174 

Trace. 
2.3 
3.1 
1.3 
4.2 

Trace. 



1.2 
36 
30 



7.57 

Trace. 

.11 

.25 

.05 

.38 

Trace. 

1.42 

5.30 

.01 

1.20 

1.00 



212 
8.2 
12 
5.7 
6.0 

2.4 

Trace. 
110 
255 

13 

27 

62 



9.22 
.21 
.60 
.47 
.21 
.22 
Trace. 

2.29 

7.21 
.10 
.90 

2.06 



188 

Trace. 

38 

10 



8.15 

Trace. 

1.90 

.82 



4.2 



.38 



713.3 



276 
2.3 

49 

78 



1.42 
7.80 
.02 
1.63 
2.59 



713.5 



1, Spring near creek; 2, swimming pool; 3, well at Calistoga Hotel. 



1 This name is said to be formed from the words California and Saratoga, but the springs are not at all like 
those of Saratoga Springs m New York. 



U. S. GEOLOGfCAL SURVEY 



WATER-SUPPLY PAPER 338 PLATE VII 




A. BYRON HOT SPRINGS, CONTRA COSTA COUNTY. 



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B. KLAMATH HOT SPRINGS, SISKIYOU COUNTY. 




C. FETTERS HOT SPRINGS, SONOMA COUNTY. 



HOT SPRINGS. 109 

The position of the springs near the base of the knoll of volcanic 
tuff that rises in the valley land and the fact that a fault has been 
traced along this part of the valley furnish suggestive evidence that 
faulting has here provided escape for deep-seated water. The lava 
may also produce a high temperature gradient that aids in giving the 
abnormal temperatures to the water. The amount of heated water 
that rises is probably better indicated by the area of meadowland 
that is formed than by the visible flow of hot water, for there is 
doubtless much seepage that is not observable. 

BYRON HOT SPRINGS (CONTRA COSTA 7). 

On the western border of San Joaquin Valley, near the southeastern 
corner of Contra Costa County, a number of mineralized springs — 
B}Ton Hot Springs — rise in a saline flat that is partly inclosed by 
low hills (PI. VII, A). A large, well-appointed hotel ^ and four or 
five cottages have here formed one of the most noted spring resorts 
of the State. The place is easily reached by automobile from the 
eastern side of San Francisco Bay. In 1908 eight springs were 
improved and used. A small warm sulphur spring supplies a drink- 
ing basin in the main grounds; warm sulphur mud and water baths 
and a sulphur plunge are about 250 yards southeast of the hotel 
grounds. A strongly sulphureted spring, 83° in temperature, forms 
a slightly used drinking pool at one side of Sulphur Plunge, and 
on the opposite side is a well from which mineral water is pumped 
to bathtubs in the hotel. In the summer of 1908 the water in this 
well stood about 8 feet below the surface and its temperature was 
112° to 115°. About 250 yards beyond the Sulphur Baths and Sul- 
phur Plunge is an inclosed swimming pool, known as the Gas Plunge, 
in which the temperature is about 88°. Between the two bathing 
establishments are two cemented drinking springs, known as the Hot 
Salt and the Liver and Kidney springs. The Hot Salt Spring, with 
a temperature of 120° and a flow of about 2 gallons a minute, rises 
in a small, domed, concrete house; the Liver and Kidney Spring 
rises in a concrete basin 25 yards southward. In 1908 its temperature 
was 73°, but its flow was not appreciable. Near the base of a low 
hill 250 yards to the southwest is a tile-lined basin or well, marked 
''Surprise," which contains strongly saline water about 70° in 
temperature. 

The following are analyses of waters from five of the springs.^ 

1 This hotel was destroyed by fire in July, 1912, but the resort was not closed, and a new hotel was 
opened in July, 1914. 

2 An iron spring, of which an analysis Is given by Winslow Anderson, could not be identified in 1908. 



110 



SPRINGS OF CALIFORNIA. 



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112 SPEINGS OF CALIFOENIA. 

The water of the White Sulphur Spring is characterized chiefly by 
primary salinity and primary alkalinity with high tertiary alkalinity. 
It is possible that the latest analysis represents a difl^erent water from 
that represented by the other two analyses, though the spring name 
is the same for all. If, however, the three analyses represent the 
same water, they indicate that a gradual loss of carbon dioxide and 
hydrogen sulphide, accompanied by mcrease in concentration, has 
been taking place. The net result of these changes has been increase 
in primary alkalinity, decrease in secondary alkalinity, and a very 
great decrease m tertiary alkalinity. 

Though the analyses of the other springs show differences in con- 
centration and m proportion of minor constituents, their waters are 
much alike m general properties of reaction, approaching sea water 
in character but differing from it in containmg a less proportion of 
magnesium and sulphate radicles. The presence of rare constituents 
in waters of such high concentration is to be expected. The water 
of the Black Sulphur Spring appears to be a relatively pure solution 
of common salt, and the "Surprise" is noteworthy for its great con- 
centration — more than nine tunes that of sea water. 

The adjacent hills are composed of cherty gravels and other finer 
sediments that represent marme deposits, but the origin and character 
of the sprmgs seem to be due to the local formation of a saline marsh. 
Several unsuccessful attempts have been made to obtam fresh water 
here, and in 1908 the domestic supply was pumped from a well If 
miles eastward. 

BOYES HOT SPRINGS (SONOMA 20). 

A number of small warm sprmgs issue along Sonoma Creek, a few 
miles north of San Pablo Bay. Artesian wells that also yield warm 
water have been drilled at several places on the eastern side of Sonoma 
Valley, and at three places where such wells have been obtained 
resorts have been built up that are well patronized durmg the summer 
months, as they are only a two and a haK hours' ride by train from 
San Francisco. Boyes Hot Sprmgs, about 2 miles northwest of 
Sonoma, is the southernmost of these resorts. Here a hotel and sev- 
eral cottages and tent houses are situated in a grove of oaks, and a 
quarter of a mile northwest of the hotel a large swimmmg plunge 
and tub baths are supplied by water pumped from two wells. These 
are said to be 200 feet deep, and the temperature of the water is 
reported to be 114° and 118°. The v/ells, the fnst of which was 
drilled about 1890, flowed until a short time after the earthquake of 
April 18, 1906, but the water usually stands a few feet below the sur- 
face. A third, unused well 300 or 400 yards to the east was flowing 
about 3 gaUons a mmute in December, 1909. The water is bottled 
for table use, and an analysis of it is tabulated (p. 113) for comparison 
with analyses of other similar waters of this valley. 



HOT SPRINGS. 



113 



OHMS SPRING (SONOMA 21). 

About Olio-half luiJo southeast of Boyos Hot Springs is another 
drilled well whose water was used to some extent in 1909 for bathing. 
The property' was open to the public under the name of Ohms Spring, 
and accommodations were provided for about 20 guests. 



AGUA CALIENTE SPRINGS (SONOMA 18). 

About 1 mile northwest of Boyes Hotel a similar resort has been 
built up at Agua Caliente Springs. A hotel and cottages here pro- 
vide for about 300 people. A large swimming plunge and tub baths 
are supplied by five flowmg wells one-third of a mile southward. 
The wells are drilled about 300 feet deep and the reported tempera- 
tures of the waters range from 97° to 108°. In 1909 Agua Cahento 
water was bottled and marketed, both carbonated and natural, for 
table use. The folloAving analyses represent the water from wells at 
Agua Caliente Sprmgs and Boyes Hot Springs: 

Analyses of water from Boyes Hot Springs and Agua Caliente Springs, Sonoma 

County, Cal. 

[Authority, advertising matter. Constituents are in parts per million.] 



Temperature 

Properties of reaction: 

Primary salinity 

Secondary salinity 

Tertiary salinity 

Primary alkalinity 

Secondary alkaUnitj' 

Tertiary alkalinity 

Constituents. 

Sodium (Na) , 

Potassium ( K) 

Lithium (Li) 

Calcium (Ca) 

Magnesium (Mg) 

Iron(Fe) 

Sulphate (SO4) 

Chloride (CI) 

Carbonate (CO3) 

Metaborate ( BO2) « 

Silica(Si0.2) 

Hydrogen sulphide (HjS) . . . 



46° C. (114° F.) 

87 


5 



41°C. (105°F.) 

SI 


9 
10 
24 



46° C. (114° F.) 

78 


9 

13 
1 



By 
weight. 



249 
8.9 
Trace. 
19 
1.0 
.5 
3.3 
369 
49 
Trace. 
103 



02.7 



Reacting 
values. 



By 

weight. 



10.83 

.23 

Trace. 

.95 

.08 

.02 

.07 

10.41 

1.63 

Trace. 

3.42 



168 
40 
3.2 
9.8 
6.0 
.7 
41 
249 
57 



646.1 



Reacting 
values. 



By 

weight. 



7.30 

1.02 

.46 

.49 

.49 

.03 

.85 

7.03 

1.91 

.05 

2.29 



173 
42 
3.2 
10 
10 

.7 
44 
256 
69 
2.5 
1.4 



611.8 



Reacting 
values. 



7.54 
1.08 
.46 
.50 
.82 
.03 
.91 
7.22 
2.30 
.06 
.05 



a Reported as boracic acid. Recalculated from H3BO3. 

1. Boyes Hot Springs, main well. Analj-st, not given. 

2. Agua Caliente Springs, well No. 3. Analyst, R. Brainard. 

3. Agua Caliente Springs, well No. 5. Analyst, J. B. Clifford 

The analyses show that the three waters are much alike in concen- 
tration and character; that is, all are primary saline waters having 
secondary and primary alkahnity as minor properties. The rela- 
35657°— wsp 338—15 8 



114 SPRINGS OF CALIFORNIA. 

lively higli proportion of silica in the first two is noteworthy. It 
is not unlikely that the third also is characterized by a high proportion 
of silica, and that a typographical error in the analytical statement 
is responsible for its apparently low silica content. 

FETTERS HOT SPKINGS (SONOMA 19). 

During the summer of 1909 a bathing establishment which is sup- 
plied by four drilled wells was erected about 200 yards east of the 
Agua Cahente baths. A hotel was opened on the grounds and the 
place was advertised in 1910 as Eleda Hot Springs, but it has since 
become known as Fetters Hot Springs (PI. VII, C, p. 108). 

The hiUs that border the eastern side of Sonoma Valley are of rhyo- 
litic lava, and the wells at the several resorts are drilled into volcanic 
tuff that underlies the thin layer of alluvium in this part of the valley. 
The presence of the lava, which is thought to be of a relatively recent 
geologic period of effusion, suggests that a rather high temperature 
gradient accounts for the thermal character of the waters and that 
the structure probably furnishes the artesian conditions. 

WARM SPRINGS OF STATE HOME AT ELDRIDGE (SONOMA 16). 

Warm springs that seem to be similar in origin to the artesian 
waters of the resorts just described issue at several points north of 
Sonoma VaUey. At the vegetable and dairy farm of the State Home 
at Eldridge water 72° in temperature is obtained from a spring that 
yields about 10 gallons a minute of water that is used in the dairy 
and for irrigation. The water broke forth at this spring at the time 
of the earthquake of April 18, 1906, and a flowing well 50 yards north- 
ward ceased to flow. A Hght-colored tuffaceous rock is exposed a few 
yards from the spring. 

LOS GUILICOS V7ARM SPRINGS (SONOMA 15). 

On the banks of Sonoma Creek, about 1^ mUes southwest of Ken- 
wood are two springs which yield, respectively, about 2 and 3 gallons 
a minute of water at temperatures of 78° and 82°. In 1909 there 
was a small bathing pool and an old hall or pavilion at the spring near 
the eastern bank of the creek; at the other spring, on the opposite 
bank, there was a small pool inclosed by an old bathhouse. The 
place was used as a camping resort, and several cot^tages had been 
erected among the trees near by. 

WARM SPRINGS ON McEWAN RANCH (SONOMA 14). 

Large warm springs that are probably similar in origin to the Los 
Guilicos springs and others farther south, issue on the McEwan ranch, 
about IJ miles west of Los Guilicos Warm Springs. A part of their 



HOT SPRINGS. 115 

yield is used for irrigation, but the springs have not been efficiently 
developed and improved. 

The hilly country several miles southeast of Santa Rosa is com- 
posed largely of lavas, and it is probable that tuffaceous layers asso- 
ciated with tlie more compact phases of the stone afford storage for 
the warm water that issues on the McEwan ranch and in other similar 
warm springs in this region. 

MARK WEST WARM SPRmGS (SONOMA 11). 

In the canyon of Mark West Creek, about 9 miles north of Santa 
Rosa, are three warm springs that issue a few yards apart along the 
east bank of the creek and supply a small plunge bath and a bath- 
house containing a few tubs. The waters are not notably thermal, 
being about 65° to 85° in temperature, but the springs are most appro- 
priately mentioned in connection mth the other thermal springs of 
eastern Sonoma County. The waters of the three springs are notice- 
ably sulphureted. On the west edge of the creek a small, cool, 
sulphur spring forms a drinking pool, and five other cool mineral- 
ized springs issue on the property. Of these. Magnesia Spring 
forms a drmking pool at the creek side near the baths, and two 
others, known as Arsenic and Iron springs, seep from a tuffaceous 
bank in a small gulch north of the main grounds. On the west bank 
of the creek, below the ba.ths, are two other small iron-stained pools. 

The Mark West springs have been improved as a resort since 1880 
or earher. In 1909 accommodations were provided chiefly by tents 
and it was visited mainly as a boating and fishing resort. 

The rocks of tliis region consist of lavas and associated tuffs that 
are similar to those near Sonoma. A high temperature gradient, 
due to the presence of the lava, possibly exists along this part of 
the coastal ranges and may be the main cause for the rise of warm 
water at Mark West Warm Springs and other warm springs in eastern 
Sonoma County. 

BIG BEND HOT SPRINGS (SHASTA 8). 

In the northeastern part of California hot springs, seemingly re- 
lated to lava flows and possibly also to local faulting that has not 
yet been recognized, issue at a number of places. Such springs rise 
along the course of Pit River, the lowermost noteworthy locality 
being at Big Bend near Henderson post office, where hot water 
issues at numerous places for a distance of about 350 yards along the 
southern bank of the river. Near the eastern end of this zone, on 
a gravel bluff about 15 yards from the river's edge, a bathhouse con- 
taining several tubs and vapor chambers has been built over one 
of the largest springs. The temperature of the water of this spring 



116 



SPRINGS OF CALIFORNIA. 



is 180° and the discharge is perhaps 25 gallons a minute. Another 
spring that yields perhaps 8 gallons a minute, of water 170° in tem- 
perature emerges at the south side of the bathhouse. These springs 
were formerly on the northern bank of a creek that entered the river 
near this point, but about 1897, to protect the springs, the discharge 
of the creek was diverted by a ditch that was cut several yards to 
the east. The stream has deepened this ditch to a steep-sided gully 
in the bed of which hot water forms pools at two places, and near its 
mouth a stream of hot water that discharges perhaps 8 gallons a 
minute issues from the gravel bluff halfway down its side. At 
places about 85 and 150 to 175 yards west of the bathhouse small 
amounts of warm water issue near or below high-water mark, and 
along the lower 65 yards of the zone of hot springs water with ob- 
served temperatures of 100° to 165° and flows of 4 to 10 gallons a 

minute issues in at 
least six places. 

The water is not 
noticeably sulphu- 
reted and, as it is 
hard, it probably 
contains a rather 
large amount of cal- 
cium. 

The upper and 
lower groups of 
springs issue from 
the gravel that bor- 
ders the river, but 
the warm seepages 
between them issue 
from a porphyritic 
quartz diorite that appears to be intruded into the old sediments 
of the locality. The hot springs probably afford a good example of 
underground water that has become heated by rock of this character. 
The position of the springs and the exposure of the intrusive rock 
at Big Bend are shown in figure 2. 

The property has been open as a resort by the present owners 
since about 1905. Accommodations for guests have been provided 
by a small hotel near the springs and in summer by tents also. The 
situation of the springs is remote, but they are yearly visited by a 
number of people who desire a quiet vacation. 

HOT SPRINGS ON KOSK CREEK (SHASTA 7). 

About 2 miles north of Big Bend Hot Springs two or three other 
thermal springs rise along the bed of Kosk Creek. One of these 
flows into a small rock basin and is occasionally used for bathing. 




500 Ft 



Figure 2.- 



-Sketch map showing positions of Big Bend Hot Springs, 
Shasta County, Cal. 



HOT SPRINGS. 



117 



In general character the springs seem to be similar to the hxrge group 
on Pit River, but their waters are not so hot and their discharges 
not nearly so large. 

BASSETT HOT SPRING (LASSEN 1). 

About 2^ miles north of east from Bieber, in Big Valley, is a hot 
spring that has been improved and for a number of years has been 
used for bathing, and as the place was formerly owned by a Mr. Bas- 
sett, it is locally known as Bassott Hot Spring. The water rises with 
a temperature of 173° from a fissure in tuffaceous sandstone that is 
exposed in a small depression 6 or 8 feet below the normal valley 
level. A pool about 20 by 40 yards across is formed here, and from 
it the water flows into another somewhat smaller pool. It is further 
cooled before reaching bathtubs in a building a few yards beyond, 
by flo\\dng in open wooden troughs. The total flow is approximately 
175 gallons a minute. The water is used for irrigating a vegetable 
garden near by, and boxes of earth that contain tomato and other 
tender plants are kept on the low tuffaceous ridge at the spring and 
are thus prevented from freezing. The water has no distinct odor 
nor taste, and the following analysis shows it to be a moderately 
minerahzed primary saline water of the sulphate type: 

Analysis of ivater from Bassetl Hot Spring, Lassen County, Cal. 
[Analyst and authority, F. M. Eaton (1909). Constituents are in parts per million.] 



Temperature 

Properties of reaction: 

Primary salinity 

Secondary salinity 

Tertiary salinity ." 

Primary alkalinity 

Secondary alkalinity 

Tertiary alkalinity 

Constituents. 

Sodium (Na) 

Potassium ( K) 

Calcium (Ca) 

Magnesium (Mg) 

Sulphate (S04) 

Chloride (CI) 

Carbonate (CO3) 

Carbon dioxide (CO2) 



78° C. (173° F.) 







6 

(?) 



By 

weieht. 



Reacting 
values. 



221 

34 

Trace. 

377 

101 

21 



757 



0.7-4 

1.68 

Trace. 

7.85 

2.85 

.70 



STONEBREAKER HOT SPRINGS (LASSEN 2). 

About 3^ miles southeast of Bassett Hot Spring a number of 
hot pools and springs rise near the southeast edge of Big Valley, 
in meadow land that formerly belonged to a Mr. Stonebreaker. 
Six pools and springs were counted in a belt extending for 275 yards 



118 SPEINGS OF CALIFORNIA. 

in a southerly direction, and between 235 and 350 yards east of the 
southernmost of these are four other hot pools. The highest tem- 
perature recorded was 165°, and the total flow, which comes mainly 
from the hottest spring, is about 125 gallons a minute. In 1909 
there was a small bathhouse at one spring ; a large warm pool was also 
occasionally used for bathing and a hot one was employed for scald- 
ing hogs. The water has been used to some extent, half a mile or more 
away, for garden irrigation. 

As at Bassett Hot Spring, the hot water of the Stonebreaker 
springs probably rises from tuffaceous sandstone that underhes the 
meadow alluvium, for the sandstone is exposed in a hill and in gulHes 
near by. Along Pit River at Bieber are good exposures of diatoma- 
ceous earth, whose presence, as well as that of the sandstone, indi- 
cates that the valley was formerly occupied by a lake. 

HOT SPRINGS IN LITTLE HOT SPRING VALLEY (MODOC 3). 

About 16 miles in a direct Hne, or 27 miles by road, northwest of 
Bieber hot water rises on the eastern side of Little Hot Spring Valley 
at two points, about 60 yards apart, at the base of low basaltic 
slopes. Much seepage water is added from a strip of marshland, and 
the resulting stream discharges about 225 gallons a minute. In the 
northern of the two springs a temperature of 127° was recorded. Its 
water is used for laundry purposes. At the lower spring, where a 
temperature of 170° was noted, a hotbed for vegetables has been con- 
structed. Like that of the Bassett and Stonebreaker springs the 
water has no noticeable odor or taste, though small amounts of cal- 
cium or magnesium salts are deposited on stones along the stream. 

Faults in Big Valley and in Little Hot Spring VaUey are not known 
to have been recognized, but the rise of comparatively pure, hot 
water in these valleys hardly indicates that the rocks are sufficiently 
open to permit atmospheric waters to reach the deeper, heated portion 
of the lava mass and then to return to the surface. 

KELLYS HOT SPRING (MODOC 4). 

Along the upper course of Pit River hot water rises at several places, 
most notably at KeUys Hot Spring (PL V, A, p. 50) 4 miles north- 
west of Canby or 21 miles west of Alturas. A pool about 12 yards in 
diameter is here formed in a semicircular depression in the alluvium 
of the northern side of the river valley. In the center of this pool 
water rises with such force as to dome up about a foot high. It is 
said that the water was formerly thrown to a height of 2 or 3 feet, but 
its action has been subdued by throwing stones into the center of the 
pool. The water has been locally considered to be several degrees 
above the boiUng point, but a temperature of 199^° in the pool 6 feet 
from its edge, at a place where the water was 1 foot deep, was the 



HOT SPRINGS. 



119 



highest measured. Water boils at 204^ at the elevation of the pool 
(4,400 feet), and it is probable that it rises with this temperature in 
the spring. The measured discharge was 32.5 gallons a minute. 
The water is used several hundred yards away as a domestic supply 
and for irrigation. A small area near the spring and between two 
outflow streams is used for growing tomatoes. The water has no dis- 
tinctly mineralized taste, though it is said to stimulate the action, 
of the kidneys. 

HOT SPRINGS ON HOT CREEK (MODOC 6). 

About 8 miles north of east from Kellys Hot Spring a stream known 
as Hot Creek is formed by numerous thermal springs that rise on the 
north side of the valley that borders Pit River. A maximum tem- 
perature of 92° was recorded here, at the side of a small house used as 
a laimdry and for bathing. The stream, which carries approxi- 
mately 700 gallons a minute, irrigates meadow land along its course 
of a mile to the river. Half a mile northeast of the main group an- 
other spring, with a temperature of 85° and a yield of about 8 gallons 
a minute, has been used to irrigate a potato field. 

WARM SPRING IN WARM SPRING VALLEY (MODOC 5). 

About halfway between Kellys Hot Spring and the springs on Hot 
Creek, a spring issues in Warm Spring Valley on gentle slopes that 
border a northern extension of the valley along Pit River. The 
temperature measured in this spring was 81°, and its flow was 
approximately 275 gallons a minute. The water is employed for 
domestic uses as well as for irrigation. The following analysis shows 
it to be a slightly minerahzed water of the primary alkaUne type: 

Analysis of vMter from spring in Warm Spring Valley, Modoc County, Cat. 
[Analyst and authority, F. M. Eaton (1909). Constituents are in parts per million.] 



Temperature 

Properties of reaction: 

Primary salinity 

Secondary salinity 

Tertiary salinity 

Primary alkalinity 

Secondary alkalinity 

Tertiary alkalinity 

Constituents 

Sodium (Na) 

Potassium (K) 

Calcium (Ca) 

Magnesium (Mg) 

Sulphate (SOi) 

Chloride (Cl) 

Carbonate (CO3) 

Carbon dioxide (CO2) 



27° C. (81° F.) 

30 



64 
6 

(?) 



- By 
weight. 



55 

3.1 
Trace. 

7.4 
22 
53 



Reacting 
values. 



2.40 

.15 

Trace. 

.15 

.62 

1.77 



140.5 



.00 



120 SPRINGS OF CALIFOENIA. 

This analysis probably also represents the general character of the 
springs of Hot Creek and also of Kellys Hot Spring. 

WARM SPRINGS NEAR RATTLESNAKE CREEK (MODOC 8). 

Warm springs that are similar to those of Hot Creek and Warm 
Spring Valley issue along the slopes that border Rattlesnake Creek, 
about 7 miles above its junction with Pit River and 8 or 9 miles (by 
road) northwest of Alturas. They form a small area of natural 
meadow land but have not been developed so as to water it efficiently. 

WARM SPRINGS NEAR CANYON CREEK (MODOC 7). 

Near the head of Canyon Creek, south of the valley of Pit River, 
warm springs that are similar in character to those already men- 
tioned in this region are used to irrigate a small amount of land on a 
ranch. 

The region including the five groups of thermal springs last de- 
scribed forms a rather mountainous plateau covered with lava. 
Faults near the- springs are not mapped on Plate III (in pocket), 
but crustal movement is suggested by the unusually high tempera- 
ture of Kellys Hot Spring, and the rise of heated waters at this and the 
other thermal springs of the region may perhaps be ascribed to the 
heat of the lavas themselves. 

KLAMATH HOT SPRINGS (SISKIYOU 7). 

Klamath Hot Springs form an isolated group near the north- 
central edge of the State. The springs rise in meadow land that bor- 
ders Klamath River near the mouth of Shovel Creek and were for- 
merly known as Shovel Creek Mud Springs. The property has been 
improved as a resort for more than 20 years and is much visited for 
the fishing that is afforded by the river, as well as for the benefit 
derived from the baths. In 1909 the improvements included a two- 
story stone hotel (PI. VII, B, p. 108) and four cottages, besides 
bathing facilities. 

Five springs and tule-grown pools are formed by the rise of thermal 
water in a meadow on the south side of the river, and two other small 
springs issue near the northern bank of the stream. Three springs 
on the southern side are those chiefly used. The hottest of these, 152° 
in temperature, forms a small drinking spring near the river and about 
175 yards from the hotel. There is a small bathhouse at another hot 
spring near by, and the main bathhouse is 100 yards to the southwest, 
at the border of a tule area. Hot-mud baths and also clear-water 
baths are here furnished by water that rises in the marshy area. The 
follomng are analyses of the main drinking and bath springs: 



HOT SPRINGS. 



121 



Analyses of water from Klamath Hot Springs, Siskiyou County, Cal. 
[Analyst, William Irelan, jr. (1896). Authority, advertising matter. Constituents are in parts per million.] 



Temperature 

Properties of reaction: 

Primary salinity 

Secondary sa 1 inity . . , 

Tertiary .salinity 

Primary alkalinity. . 
Secondary alkalinity 
Tertiary alkalinity. . , 



69° r. (156° F.) 

76 
20 


4 



44° C. (112° F.) 

66 
5 



29 

7 



Constituents. 



By 
weight. 



Reacting 
values. 



By 
weight. 



Reacting 
values. 



Sodium (Na) 

Potassium (K). . . . 

Lithium (Li) 

Calcium (Ca) 

Magnesium (Mg). . 

Iron(Fe) 

Sulphate (SOi) 

Chloride (CI) 

Carbonate (CO.,) . . 
Metaborate (BO«) . 
Silica (SiOs) 



543 

4.8 



23.60 
.12 



143 
2.9 
4.1 

365 

788 

60 
82 



7.13 
.24 
.15 

7.62 

22. 23 

.00 

1.39 

2.72 



443 

1.4 

Trace. 

183 

12 

1.8 

337 

490 

241 

27 

63 



19.28 

.04 

Trace. 

9.13 

.99 

.06 

7.02 

13.82 

S.OJ 

.63 

2.09 



1,992.8 



1, 799. 2 



1. Hottest drinking spring; 2. Main bath spring. 

The analyses represent primary saline waters of the chloride type, 
the drinking spring being characterized by secondary salinity and tho 
bath spring by secondary alkalinity. Tertiary alkalinity is not fully 
reported. The presence of borates in both springs is noteworthy. 

Along this portion of its course Klamath River has cut a wide 
canyon, 1,200 feet or more deep, into lava. Prominent bluffs of 
tuffaceous material are exposed along its north side one-third of a 
mile west of the Klamath springs. Faulting might again be appealed 
to in an attempt to explain the rise of the thermal water here, but it 
is possible that an abnormal temperature gradient in the bottom 
of this deep canyon in the lavas, combined with local fracturing or 
with the presence of porous beds that allow the escape of deep-seated 
water, may furnish a satisfactory explanation for the existence of the 
hot springs. 

HOT SPRINGS ON BIDWELL CREEK (MODOC 10). 

In the western part of the United States there is a large area from 
which no streams flow to the ocean and which is therefore called the 
Great Basin. Many of the mountain ranges and intervening vaUeys 
in this area have been formed by extensive faulting, a mode of forma- 
tion here so common that its result is loiown as "Basin Range" 
structm'e. One of the minor divisions of the Great Basin along the 
northeast border of California is Surprise Valley, whose formation 



122 



SPRINGS OF CALIFORNIA. 



was ascribed by Russell ^ to faulting along both sides of the valley, 
subsidiary faulting having produced its minor features. The hot 
springs that rise in the valley are considered to furnish confirmatory 
evidence of its fault origin. 

The northernmost of the hot springs that are noteworthy are 
found at the base of lava slopes on the west side of the canyon 
of Bidwell Creek, about 1 mile north of Fort Bidwell. From five 
vents within 6 or 8 yards of each other about 75 gallons of water a 
minute is discharged, the highest recorded temperature being 108°. 
In 1909 the water was conducted to a plunge in a small bathhouse 
and was also used for irrigation and domestic supply. 

On standing the water deposits a small amount of sulphur. The 
following analysis shows that the water is characterized by primary 
alkalinity and primary salinity and, to a small degree, by secondary 
alkalinity. Tertiary alkalinity, though not fully reported, is impor- 
tant. The softness of the water and its suitabihty for use in laun- 
dries is recognized, and it is a good boiler water but is only fair for 
irrigation. 

Analysis of ivater from main hot springs on Bidwell Creeh, Modoc County, Cal. 
[Analyst and authority, F. M. Eaton (1909). Constituents are in parts per million.] 



Temperature 

Properties of reaction: 

Primary salinity 

Secondary saUnity . . 

Tertiary salinity 

Primary alkalinity. . 
Secondary alkalinity 
Tertiary alkalinity . . 



38° C. (100° F.) 

47 


42 
11 
58 



Constituents. 



By 
weight. 



Reacting 
values. 



Sodium (Na)... 
Potassium (K). 
Calcitun (Ca)... 
Magnesium (Mg). 
Iron r 



. (Fe). 



Aluminum ( Al) . 
Sulphate (SO4)... 

Chloride(Cl) 

Carbonate (CO3) . 
Silica (Si02) 



Carbon dioxide (CO2) 

Hydrogen sulphide (H2S) . 



78 
7.7 
3.7 
2.9 

2.8 

58 
24 
62 
65 



Present. 

2.8 



3.39 
.20 
.18 
.24 

.10 
1.20 

.69 
2.08 
2.15 



Present. 
.16 



HOT SPRINGS NEAR SOUTHWEST SIDE OF UPPER LAKE (MODOC 11). 

At points about 2 miles and 3 miles, respectively, north of Lake 
City, hot water rises in meadowland that borders Upper Lake. The 
quantity of flow and the temperature of the water are rather indefi- 
nitely known, as the water rises in tule-grown areas. It has been 

1 Russell, I. C, A geological reconnaissance in southern Oregon: U. S. Geol. Survpy Fourth Ann. 
Rept., pp. 449-450, 1884. 



HOT SPRINGS. 12.S 

used luainly for irrigutiug tlio ineadowland, but the supply could be 
developed and more efficiently used by proper ditching. 

HOT SPRINGS ON EAST SIDE OF SURPRISE VALLEY (MODOC 14). 

Between Upper and Middle lakes, on the east side of Surprise Val- 
ley, three small hot springs rise in a small depression on a gentle 
greasewood-covered slope. The discharge from the springs is 
increased by seepage from a marshy strip along the overflow, 75 or 
100 yards beyond. In 1909 the water was used for irrigating meadow- 
land and a small vegetable garden. The soil near the springs showed 
an efflorescence of common salt and soda, but the water did not taste 
noticeably mineralized. 

HOT SPRINGS AT EAST BORDER OF SURPRISE VALLEY (MODOC 13), 

One mile west of the hot springs between Upper and Middle lakes 
near the base of slopes that encroach on the valley, scalding water issues 
from small vents within a space of 20 yards. Corrals and vats have 
been constructed here and the water has been used in preparing sheep 
dip. The water is without appreciable odor or taste and is not 
notably mineralized. About 100 yards east of the springs is a ledge 
of iron-stained silicified rock that resembles in appearance an ande- 
sitic dike rock that has been silicified by the action of heated water. 
A prospect pit for limestone has been dug in a small deposit of calcare- 
ous tufa, half a mile southward, but this material was not observed 
at the springs. 

HOT SPRING NEAR EAST SIDE OF MIDDLE LAKE (MODOC 15). 

Near the eastern side of Middle Lake is a hot spring that is said to 
form a pool 25 feet in diameter and 6 feet deep. Its flow has been 
estimated at more than 300 gallons a minute, and like the other 
springs of the valley it forms a meadow area bordering the lake. 

HOT SPRINGS NEAR WEST SIDE OF LOWER LAKE (MODOC 16). 

About 5 miles south of Eagleville hot water issues at half a dozen 
or more places in the gravel of the valley side, in a depression similar 
to the depressions in which other hot springs in Surprise Valley issue. 
The water has no appreciable taste or odor. There was formerly a 
small bathhouse at these springs, and later a dam was constructed 
that made a swimming pool, but in 1909 the water was used only to 
irrigate 30 or 40 acres of meadow and alfalfa. 

HOT SPRINGS NEAR SOUTHWEST SIDE OF LOWER LAKE (MODOC 17). 

Three miles south of the springs just described is another group of 
hot springs that are said to irrigate about 160 acres of meadow. The 
water at this place forms a pool and is considered to be somewhat 



124 SPRINGS OF CALIFORNIA. 

warmer than that of the springs a few miles northward. There are 
also several small warm springs near the road between these two 
groups of springs. 

WARM SPRINGS AT SOUTH END OF SURPRISE VALLEY (MODOC 18). 

A small amount of warm water rises in meadowland at the south 
end of Surprise Valley. This water may rise along a fault zone, as 
the principal springs of the valley are considered to rise, but it may 
also be of alluvial artesian character. 

BOYD SPRING (MODOC 12). 

Boyd Spring is marked on some maps as Boyd Hot Spring, but its 
recorded temperature in 1909 was only 67°. The water has no 
noticeable taste, and in several respects it seems to be a spring of 
alluvial artesian origin rather than one whose existence is due to the 
rock structure. It is mentioned with the hot springs of Surprise 
Valley, however, because it is to some extent thermal and may have 
a structural origin. It is situated near the eastern side of Upper Lake, 
on a gentle greasewood-covered slope. A tule-grown pool has formed 
here, about 15 by 25 yards in dimensions, in which there are many 
small fish. The discharge flows westward in a sluggish stream of 
perhaps 1,000 gallons a minute, though at the point where the stream 
was measured the current was so shght that its volume could be only 
roughly approximated. In 1909 it was used for irrigating meadow 
half a mile or more to the northwest. 

SHAFFER HQT SPRINGS (LASSEN 16). 

In Honey Lake valley there are two large groups of hot springs — 
one, the more interesting, near Hot Springs railroad station and the 
other near Amedee. At the former locality, near the northeastern 
side of Honey Lake, a belt of calcareous tufa extends from the base 
of steep slopes that border the valley near the railroad station south- 
westward for nearly half a mile. The continuity of the surface exposure 
of the material is then broken, but the course of the deposit is marked 
for two-thirds of a mile farther by prominent crags and knolls of the 
material that rise in meadow and salt-grass land that extends to the 
lake. One of these crags is shown in Plate VIII, A. Seepage springs 
rise at several points along the middle part of this tufa belt, but the 
springs of chief interest issue beyond its most lakeward outcrop. 
They are not known locally by a definite name, but as they were 
referred to in 1882 by Russell as Shaffer Hot Springs, this name is 
here used. 

The principal spring rises with vigorous ebulhtion in a pool about 
10 yards in diameter and 1 or 2 feet deep. The water was formerly 



U. S. GEOLOGICAL SURVEY 



WATER-SUPPLY PAPER 338 PLATE VIII 







A. CALCAREOUS TUFA NEAR SHAFFER HOT SPRINGS, LASSEN COUNTY. 




B. CARBONATE DEPOSIT OF JORDAN HOT SPRINGS, TULARE COUNTY, 



HOT SPRINGS. 125 

tlirown up to a height of 3 or 4 feet, but this action has been partially 
stopped by stones that have been cast into the pool. A temperature 
several degrees above boiling has been claimed for tliis spring, but 
204°, near the center of the pool, was the highest temperature re- 
corded. This is the same temperature at which water boiled in a 
bucket over a fire near the spring and is practically the calculated 
boihng point for this elevation (3,975 feet). A bathhouse that 
extended o\^er a part of the pool was in 1909 used as a vapor bath. 
In 1882 Russell ^ estimated the flow of this spring to be 100 cubic feet 
a minute (748 gallons a minute), but in September, 1909, the average 
of three float measurements indicated a discharge of only about 175 
gallons a minute. It does not seem probable that this great difference 
is due to error in measurement, and it is believed to show that the 
flow has actually decreased, possibly because of the partial choking 
of the vent with stones. Two other hot springs that discharge about 
65 and 10 gallons a minute, respectively, and 6 or more hot pools 
that have no surface outflow, are formed in the nearly level salt-grass 
area in a distance of about 125 yards southwest of the main spring. 

In his monograph on Lake Lahontan ^ Russell says of these springs 
and the associated tufa: 

This spring occurs at tlie southern end of a long row of tufa crags, fully 50 feet high 
and somewhat greater in breadth, a few of which still have small springs issuing from 
their bases. The tufa at the base of the crags, and forming the nucleus of the deposit, 
is amorphous, but is coated with a heavy deposit of the dendritic variety. * * * 
The former was a direct precipitate from spring water, but the latter was plainly 
deposited from the former lake. The evidence is such as to lead to the conclusion 
that this spring was fully as copious during the existence of Lake Lahontan as now, 
and that its point of discharge was crowded southward along a fissure as its former 
outlets became filled with calcareous tufa deposited from its own waters. 

Russell also gives an analysis of the water, which is here reproduced, 
together with analyses that were made of the spring and lake waters 
in 1909. The analyses show that the spring water is a primary saline 
solution containing a large proportion of silica. The comparatively 
small amounts of calcium and carbonate present are of interest 
with respect to the large tufa crags, but calcium carbonate is easily 
formed and precipitated, so that large amounts are not necessarily 
present for the production of prominent deposits. The lake water is 
characterized by primary alkalinity as well as primary salinity. 

1 RnssoU, I. C, Geological history of Lake Lahontan: U. S. Geol. Survey Mon. 11, p. 51, ^885. 

2 Lake Lahontan is the name that has been given to a body of water that occupied Honey Lake 
Valley and adjacent valleys during early Quaternary time. 



126 



SPEINGS OF CALIFORNIA. 



Analyses ofxvaterfrom Shaffer Hot Springs and Honey Lake, Lassen County, Cal. 
[Constituents are in parts per million.] 



Properties of reaction: 

Primary salinity 

Secondary salinity. . . 

Tertiary saiinity 

Primary alkalinity. . . 
Secondary alkalinity . 
Tertiary alkalinity . . 



(?) 



Constituents. 



By Reacting 
! weight. values. 



By 
weight. 



Reacting 
values. 



weight. 



Reacting 
values. 



Sodium (Na) 

Potassium (K) 

Calcium (Ca) 

Magnesium (Mg).. 
Sulphate (SO4).... 

Chloride (CI)...... 

Carbonate (C03).. 
Metaborate (BO2). 
SOica(SiOo)....... 



349 

207 



13.22 

.24 
.60 
.03 

7.27 
5.84 



353 

203 



7.32 
5.73 



131 



Trace. 
120 



Trace. 
3.98 



622 

21 

7.9 

264 

365 

383 



27.04 

1.05 
.65 

5.50 
10.29 
12.78 



1,012.8 



1,662.9 



Carbon dioxide (COo). 







1. Main spring, Shaffer Hot Springs. Analyst, F. W. Clarke (1883). Authority, U. S. Geol. Survey 
Bull. 9. 

2. Main spring, Shaffer Hot Springs. Analyst, G. E. Colby (1909). Authority, owner of springs. 

3. Honey Lake. Analyst and authority, F. M. Eaton (1909). Sample collected 75 yards from north- 
east shore, where water was 18 inches deep. 

Dana^ has made aclose examination of the calcareous tufa deposited 
in the basin of Lake Lahontan. Three varieties are recognized, 
which differ chiefly in physical characteristics. The variety at 
Shaffer Hot Springs, which assumes mushroom shapes, is much the 
commonest and is known as dendritic tufa. An analysis of the ma- 
terial is here reproduced, because, though not strictly a hot spring 
deposit, the crags near Shaffer Hot Springs are evidently closely 
related to the presence of the hot water. 

Analysis of dendritic tufa from basin of Lake Lahontan. 

[Analyst, D. O. Allen (1882 ?). Authority, U. S. Geol. Survey Mon. 11, p. 203.] 

Insoluble residue 5. 06 

Iron and alumina (FegOg+AljOg) 1. 29 

Calcium oxide (CaO) 49. 14 

Magnesium oxide (MgO) 1. 99 

Chlorine (CI) Trace. 

Sulphate (SO4) Trace. 

Phosphate (P2O5) Trace. 

Carbon dioxide (CO2) 40. 31 

Water (H2O) 2. 01 

99. 80 



1 Dana, E. S., A crystallographic .study of the thinolite of Lake Lahontan: V. S. Geo!. Survey Bull. 12, 
1884. 



HOT SPRINGS. 



127 



AMEDEE HOT SPRINGS (LASSEN 17). 

The second group of hot springs in Honey Lake Valley is about 5 
miles southeast of Shaffer Hot Springs, near Amedee depot. The land 
here is alluvial and slopes very gently westward toward Honey Lake. 
Scalding water forms several groups of shallow pools, mainly at 
six places in a belt about 600 yards long that trends nearly south- 
ward, but one-third of a mileS. 30° W. (magnetic) from the southern- 
most of these main groups another hot spring forms a pool in salt- 
grass land, and hot water probably rises at other places still farther 
toward the lake. Temperatures of 172° to 204° (practically the boil- 
ing point at this elevation, 4,000 feet) were noted in the several 
springs, and the total discharge of hot water as measured by the flow 
of six run-off streams is about 700 gallons a minute. 

In 1909 the springs had not been improved to great extent, but 
there was a small bathhouse beside the railroad, near one of the 
largest groups of springs. At the southernmost of the main groups 
there was also an old bathhouse, and water from one of the northern- 
most springs was used in preparing sheep dip. At the Amedee Hotel 
a shallow well 80 yards east of the nearest springs supplied water at 
a temperature of 134° for kitchen use. 

There are no prominent deposits of tufa at Amedee, such as there 
are near Shaffer Hot Springs, but near the southernmost of the main 
groups tufa appears over a small area. The hottest spring rises from 
this material. The following analysis of the water from this spring 
shows that it is a primary saline water almost identical in character 
with that of the Shaffer spring but of slightly less concentration. 

Analysis of water from Amedee Hot Springs, Lassen County, Calfl 
[Analyst and authority, F. M. Eaton (1909). Constituents are in parts per million.) 



Temperature 

Properties of reaction: 

Primary salinity 

Secondary salinity 

Tertiary salinity 

Primary alkalinity 

Secondary alkalinity 

Tertiary alkalinity 

Constituents. 

Sodium (Na) 

Potassium ( K) 

Calcium (Ca) 

Magnesium (Mg) 

Iron (Fe) 

Aluminum (Al) 

Sulphate (S0<) 

Chloride (Cl) 

Carbonate (CO3) 

SiUca (Si02) 

Carbon dioxide (CO2) 

a Spring 150 yards southwest of Amedee depot 



90° C. (204° F.) 

91 


1 



By 
weight. 



Reacting 
values. 



232 
4.9 
18 
Trace. 

1.8 

269 
164 

27 

94 



10.18 

.13 

.90 

Trace. 

.06 

5. CO 

4.62 

.91 

3.12 



810.7 



Present. 



Present. 



128 SPRINGS OF CALIFOKNIA. 

HIGHROCK SPUING (LASSEN 19). 

A large thermal spring rises on the Highrock ranch, about 10 miles 
south of east from Amedee. Its water is used for domestic supply 
and for irrigation, and the spring forms a convenient watering place 
on the road between Honey Lake Valley and Reno, Nev. Measure- 
ments in 1909 showed its flow to be about 525 gallons a minute and 
its temperature 86°.^ The water does not have a distinctive alkaline 
taste, but it is said to rust tinned-iron vessels quickly. 

The spring rises at the edge of Honey Lake Valley, from basaltic 
lava that forms the hills to the east. No deposit of note is observ- 
able immediately at the spring, but 30 yards northwestward are 
prominent calcareous tufa crags from which the ranch takes its name. 
The deposit covers an area of perhaps 2 or 3 acres, and its well- 
developed crags are coated with dendritic tufa. Water does not now 
issue from the tufa, but there is said to be an Indian legend that the 
main spring formerly did so. 

KRUGER SPRING (PLUMAS 11). 

At the upper end of Indian Valley in Plumas County, in meadow- 
land a mile east of Greenville, there is a thermal spring that has been 
known as Kruger Spring since the late eighties. During the more 
prosperous days of mining in this region it was extensively patronized 
as a bathing place. Of late years, however, the bathhouse has not 
been kept in repair and it has not been open to the public. In 1909 
about 1 gallon a minute of water 94° in temperature flowed from a 
board-curbed pool in the bathhouse. Both the temperature and the 
yield could probably be increased by sinking a well casing into 
the spring. A few bubbles of gas rise in the pool, but the water has 
no distinctive taste or odor. The spring may furnish evidence that 
there has been faulting through Indian Valley. It seems more prob- 
able, however, that alluvial artesian water is here brought to the 
surface, possibly by a buried ridge. 

MARBLE HOT WELLS (PLUMAS 16). 

In Sierra Valley, in the southeastern part of Plumas County, several 
flowing artesian wells discharge water of unusually high temperature. 
The most remarkable of these wells are on the Marble ranch, at Kettle 
post office, where, in 1885 and 1888, two wells, 4 inches in diameter, 
were sunk about 100 yards apart to a depth of 350 feet. Each of 
these wells discharges about 175 gallons a minute of scalding water, 
the recorded temperatures being 156° and 161°. A third well, 150 
yards west of the other two, was sunk to a depth of 450 feet, at which 

1 In 1882 Russell reported its temperature to be 100° (U. S. Geol. Survey Mon. 11, p. 52), but it is doubtful 
whether such a marked reduction in temperature has really taken place. 



HOT SPRINGS. 129 

(lopth the drill oiicountered ''quartz/' possibly bedrock. The well 
did not yield a large flow. In 1909 its discharge was about 1 gallon 
a minute, and the temperature of the water was 125°. 

About 350 yards north of the northernmost well is a spring that 
formerly yielded hot water, but its flow and temperature were reduced 
by a well, since abandoned, that was sunk a short distance north of 
it. When this spring was visited it formed a pool from which there 
was a flow of perhaps 3 gallons a minute. The highest temperature 
recorded in it was 87°. 

Water from the two principal wells is used for domestic supply and 
for irrigation. It is considered to be of good quality, though it acts 
as a laxative. An examination of the water by Mr. J. W. Montague, 
a chemist of San Francisco, has shown that it contains 1,400 parts 
per million of solids in solution. Of this amount, 40.81 parts are 
reported as sodium chloride (common salt). Small incrustations of 
calcium or magnesium carbonate form on the discharge pipes. The 
fact that the water will deposit a rust-colored stain on clothes that 
are allowed to soak in it for some time indicates that it contains also 
a noticeable amount of iron. Baths have been provided and they 
are occasionaUy used for relieving rheumatism, but when visited in 
1909 no attempt had been made to develop the property as a bathing 
resort. About 6 miles southeast of the Marble wells is another hot 
well, but its flow is smaller and the temperature of its water is lower. 

Several other flowing wells that yield warm water are situated 
along a belt that extends for several miles southeastward. 

A fault that passes through Sierra Valley has been mentioned by 
Diller ^ and by Turner ^ and is shown on Plate III (in pocket). The 
movement along this fault is considered to account for the existence 
of hot water beneath the valley, as the fracturing has probably fur- 
nished places for the escape of deep-seated water upward into the 
alluvium. 

CAMPBELL HOT SPRINGS (SIERRA 1). 

At the extreme southern border of Sierra Valley, about 2 miles by 
road southeast of Sierraville, eight thermal springs are scattered for 
a distance of a mile along the low slopes that border this end of the 
valley and in the adjacent meadowland. The property has been 
improved as a resort since tlie early eighties, and in 1909 a three-story 
hotel and an annex provided accommodations for 100 guests. 

One of the largest hot springs rises on the hillside, 50 feet above the 
valley. It discharges about 15 gallons a minute of shghtly sulphu- 
reted water 102° in temperature. The water has been piped to tubs 

1 Diller, J. S., Notes on the geology of northern California: U. S. Geol. Survey Bull. 33, p. 14, 1886. 

2 Turner, H. W., Mohawk lake bods: Thitos. Soc. Washington Proc, vol. 2, pp. 396-397, 1892. 

35657°— wsp 338—15 9 



130 



SPRINGS OF CALIFORNIA. 



and to a plunge, and has also been used for garden irrigation. Water 
from another spring that rises at the edge of the meadow, 800 yards 
to the southeast, has been used to supply a wooden swimming plunge 
near by. The observed temperature of this sprin-g was 98° and its 
flow was about 30 gallons a minute. Its water is more noticeably 
sulphureted than that of the first-mentioned spring, and it also has 
a corrosive effect on the boards that curb it. 

A cool spring beside the hotel and another at camp grounds to the 
southeast have been used for drinking. The other springs have been 
slightly used for irrigating vegetable patches. The water of one of 
them, called the Hobo Spring, issues with a temperature of 111°, 
which is the highest that was observed in this group. An old bath- 
house at the westernmost spring was apparently little used. 

The following are analyses of water from the main hot spring and 
the cool spring at the hotel : 

Analyses of ivater from Campbell Hot Springs, Sierra County, Cat. 
[Analyst, not given. Authority, advertising matter. Constituents are in parts per million.] 



Temperature 

Properties of reaction: 

Primary salinity 

Secondary salinity 

Tertiary salinity 

Primary alkalinity 

Secondary alkalinity 

Tertiary alkalinity 

Constituents 

Sodium (Na) 

Calcium (Ca) 

Magnesium (Mg) 

Iron(re) 

Aluminum (Al) 

Sulphate (SO4) . 

Chloride (Cl) 

Carbonate (COs) 

SUica (Si02) 



Main hot spring. 



40° C. (104° F.) 

54 
38 


8 
70 



Cool spring. 



By 
weight. 



Reacting 
values. 



weight. 



Reacting 
values. 



143 
75 
14 

117 



3.00 

2.19 

.37 

.75 

2.98 
2.11 

.47 
3.88 



97 
44 
4.2 



154 
70 



116 



4.22 

2.19 

.35 

.47 

3.20 
1.96 
1.60 

3.85 



546.2 



The analyses indicate that these two springs yield waters of the 
same general type, but the water of the cool spring is characterized 
by greater proportions of primary bases and alkahnity as well as 
somewhat greater concentration. 

The hiUs near the springs are of lava that is probably andesite. 
The fault that passes through Sierra Valley has been mapped on 
Plate III (in pocket) as passing close to the Campbell Hot Springs. 
Hence the origin of the hot springs, like that of the hot weUs farther 
north, seems to be properly assigiaed to the presence of this struc- 
tural break, through which deep-seated water rises. 



HOT SPRINGS. 131 

BROCKWAY HOT SPRINGS (PLACER 8). 

The only noteworthy thermal springs in the basin of Lake Tahoe 
are at the north end of the lake, near Statehne Point, at a fishing and 
boating resort, known as Brockway, where in 1909 a hotel and four 
cottages provided accommodations for 100 })eu})lc. The springs rise 
in the lake within a few feet of the shore, bubbling up from numerous 
vents, principally at two localities. One of these localities is at the 
boat pier, where one spring has been cemented so as to form a drinking 
basin near the lake edge. A temperature of 137° was recorded in 
this spring, and the discharge was about 3 gallons a minute. A plan 
had been considered for making a warm swimming pool by construct- 
ing a concrete wall around the springs in the lake at this place. 
Water from another group of springs, which is situated in the lake 
near its edge, about 150 yards northwestward, is pumped to a tank 
near by and used for bathing and for laundry purposes. The water 
is faintly sulphureted but seems to be only slightly mineraUzed other- 
wise, for it is very soft and excellent for laundry use. 

The springs rise from granodiorite which is overlain on the slopes 
above by andesitic lava. A probable fault has been mapped by 
Lindgren ^ as passing southeastward through the lake, about one- 
tliird of a mile west of the springs. ^ This fault appears to furnish 
the most plausible explanation for the existence of the springs. 

GROVERS HOT SPRINGS (ALPINE 1). 

In Alpine County, about 4 miles west of Markleeville and near the 
southern extension of the Sierra Valley fault, considerable heated 
M^ater rises at Grovers Hot Springs from a dozen springs and seepages 
in two marshy areas about 100 yards apart, at the edge of a meadow 
on the southern side of Markleeville Creek. The principal springs 
range in temperatm^e from 128° to 146° and their combined dis- 
charge — perhaps 100 gallons a minute — hrigates the meadow. 

In 1909 a pool 3 or 4 feet deep and about 30 feet square was used 
for bathing, and the place has been visited as a camping resort for 
many years. 

Lime carbonate has been deposited by the springs and is especially 
noticeable below several of the springs that flow down over a terrace 
or bank that has probably been foiiiied by the carbonate material. 
The slopes that surround the springs are granitic, but less than half a 
mile to the east there is lava that possibly has some relation to the 
hot water and to its content of lime carbonate. The fact that an 
extensive fault passes close to the springs suggests, however, a more 
plausible cause for the issuance of the hot water. 

' Lindgren, Waldemar, U. S. Geol. Survey Geol. Atlas, Truckee folio (No. 39), 1S97. 
2 This fault is not shown on map No. 1 of the atlas accompanying the report of the California State Earth- 
quake Commission, probably through oversight. 



132 SPRINGS OF CALIFOENIA. 

FALES HOT SPRINGS (MONO 1). 

Fales Hot Springs are about 13 miles northwest of Bridgeport, on 
the main road to Minden, Nev. In 1908 there was a stage station 
and road house at the place, and plunge and tub baths were provided 
for use of the water. The place was too inaccessible to have become 
much of a resort, but during the summer months it was visited by 
campers. 

The hot water rises along the bed of a small creek that has been 
dammed to form a bathing pool and to keep the water at a com- 
fortable temperature, for in the main group the temperature ranges 
from 129° to 141°. Measurements indicated that the total discharge 
was about 300 gallons a minute. Much gas, probably carbon dioxide, 
rises with the water, which is too hard for use in laundry work. 
Hard, shiny nodules occasionally found in the creek are probably 
composed mainly of lime carbonate, though they may contain con- 
siderable silica. No other deposit of note is formed at the springs, 
but on the hillside 400 yards north of east from and 125 feet higher 
than the present springs there is a circular lime-carbonate basin, about 
100 feet in diameter and 25 feet deep, with a rim 50 to 150 feet thick. 
Another smaller lime carbonate deposit lies halfway between this 
basin and the springs, and a third deposit of the same material ap- 
pears along the creek side 250 to 400 yards east of the springs. Hot 
water no doubt formerly issued at these places and built up the 
deposits. 

The region east of the springs and apparently the higher slopes 
that surround them are granitic, but the slopes near by are of lava. 
Less than 50 yards northwest of the springs is a knoll of lava that is 
considered by E. S. Larsen, jr., to be quartz latite. Along the creek 
banks on each side of this material the rock has been so completely 
decomposed to a clay as to suggest that the lava is an intrusive mass 
or dike. If this is true, it is probable that the heat of the water and 
also its chemical contents are derived from the lava. The association 
of lava with lime carbonate deposits at hot springs has been mentioned 
in the descriptions of a few other springs, and seems worth calling 
attention to again in connection with the springs at Fales. 

BUCKEYE HOT SPRING (MONO 2). 

Buckeye Hot Spring is about 5^ miles south of west from Bridge- 
port and on the north bank of Buckeye Creek, a mile above the mouth 
of its canyon and 40 feet above the stream. The water issues with a 
temperature of 140°, and perhaps 25 gallons a minute flows down to 
the creek over a large domelike overhanging deposit of lime carbonate. 
In 1908 a part of the water was conducted across the creek in a small 
trough to a cabin in which there were two wooden bathtubs; but 



HOT SPRINGS. 133 

apparently the place was not often visited. The water has no appre- 
ciable taste or odor, but the large deposit of lime carbonate indicates 
that it carries notable amounts of the constituents of that material. 
The carbonate is deeply iron stained near the spring, so the water 
probably contains also a fairly high amount of iron in solution. 

The formation near the spring seems to be a terrace composed of 
granitic bowlders and finer material. No direct evidence of the 
origin of the springs was obtained, but as they lie along the eastern 
front of the Sierra, where extensive faulting has taken place, it seems 
probable that at this place, as at so many others, faulting has pro- 
vided a means of escape for heated water. 

WARM SPRINGS NEAR BRIDGEPORT (MONO 4). 

About 1^ miles south of Bridgeport are other hot springs that 
have formed noteworthy deposits of lime carbonate. At this locality 
there are about 20 pools, ranging in diameter from about 10 inches 
to 10 yards, that are scattered for a distance of 350 yards along a 
terrace that borders a small creek. Much gas, which is probably 
carbon dioxide, rises; but the total visible flow of the springs is 
only about 25 gallons a minute. Temperatures of 70° to 105° were 
observed in the various pools. In addition to the present pools 
there are a number of low mounds that are evidently extinct springs. 
In 1908 the springs at this place were unused, and apparently had 
not at any time been improved for bathing or other purposes. 

The slopes that rise eastward are covered with lava that is probably 
andesite. In a canyon half a mile eastward cliffs of light-colored 
siliceous tuff are exposed. 

HOT SPRINGS NEAR BRIDGEPORT (MONO 3). 

A much more noteworthy group of hot springs, similar in char- 
acter to those just described, is foiuid about l^ miles southeast 
from Bridgeport, on liilly slopes of andesitic lava, 200 to 300 feet 
above the valley. The locality of special interest is an area of gently 
sloping ground, approximately 350 yards in diameter, that lies at the 
base of steeper slopes and includes a number of prominent ridges of 
banded onyx marble or travertine,^ 5 to 15 feet high and of somewhat 
greater thicknesses, that tend to radiate from a central point, as shown 
in figure 3 (p. 134). Each of the better-developed ridges is cut longi- 
tudinally by a vertical crevice, and the banding of the travertine, 
which is stained various shades of red and yellow, is seen at several 
places to be also vertical. On the outside of several of the ridges duU- 
brown lime carbonate has formed but in nearly horizontal layers. It 
has apparently been deposited where the water has flowed out over 

' Specimens of this material have been examined microscopically by E. S. Larsen, jr., and identified as 
calcite. 



134 



SPRINGS OF CALIFORNIA. 



the ridges. The deposition of the onyx marble has apparently ceased, 

and the lime carbonate that is now being deposited is in the form of 

dull-brown tufa.^ 

In 1893-1895 a quarry was opened in one of the ridges, and about 

60 tons of the material was taken out and shipped in rough blocks 

to San Francisco. It was there 
cut into slabs and polished and 
used in the rotunda of the City 
Hall. In 1910 the deposit had 
not been worked since the San 
Francisco order was filled, as the 
nearest railroad point was 50 miles 
distant. The material has a pleas- 
ing mottled effect, is sufficiently 
translucent to give depth to the 




vf'V / -^^'^ 



-y/znWilW^^ 



\ '\\ '"''' 0^4? 



'^'I<^ 






500 1000 Feet 



FiGUEE 3.— Sketch map of travertine ridges near 
Bridgeport, Mono County, Gal. a, Bathhouse; b, 
main spring; c, derrick at quarry. 



coloring, and takes a good polish. 

At two points near these ridges 
small springs, with temperatures 
of 121° and 148°, rise in pools 
about 3 and 10 feet in diameter. 
Water from the larger pool has 
been used to some extent for bath- 
ing in a small house near by. A 
third spring issues from a longi- 
tudinal crevice in the top of one of the ridges, which is shown in 
Plate IX, A. Its temperature is also 148° and its flow is perhaps 
one gallon a minute. It deposits lime carbonate on troughs and 
barrels that have been arranged so that the water can be used in 
preparing sheep dip. This deposit is said to form at the rate of nearly 
an inch a month. The water is noticeably carbonated, and the fol- 

1 The following notes concerning the formation of travertine are abstracted from an article by George P. 
Merrill, entitled "The onyx marbles; their origin, composition and uses, both ancient and modem" 
(Smithsonian Inst. Ann. Rept. for 1893, pp. 539-585, 1895). 

Pure water dissolves only 1 part of calcium carbonate in 10,800 when cold, and 1 part in 8,875 when boiling; 
but when saturated with carbon dioxide at 10° C. (50° F.) it will dissolve nearly 1 part in 1,000 (0.88 
grams per liter). The amount is increased by increased pressure, and under the most favorable circum- 
stances the amount of calcium carbonate dissolved is 3 parts in 1,000. On cooling, and especially on relief 
of pressure and consequent escape of carbon dioxide, the excess of calcium carbonate is redeposited. Slow 
deposition tends to produce a crystalline structure; rapid deposition tends to produce a cellular one. The 
form of crystallization may also be determined by the character of the deposition, for G. Rose has shown 
(Fouqu^ and Levy, Synthese des mineraux et des roches) that by humid methods it is possible to produce 
out of the same solution crystals of both aragonite (orthorhombic, specific gravity 2.95) and calcite (hex- 
agonal rhombohedral, specific gravity 2.72), the one or the other forming according to the temperature of 
the solution. Aragonite is formed exclusively by rapid evaporation of hot solutions, while calcite may be 
produced from similar solutions, both hot and cold. Most known deposits of onyx marble apparently were 
formed by hot water that was probably of a high degree of saturation and under some pressure. Rapid, 
cellular deposition is checked and a slower, compact, crystalline one is favored if the mineralized waters 
discharge in quiet pools; hence Merrill considers this condition of formation to have been a probable one 
at onyx marble deposits. Variations in the temperature of the water, the rate of cooling, and the amount 
and proportions of calcium, iron, and bicarbonates in solution, and the presence of impurities, such as 
clay, produce the numerous banded varieties of the stone. 



U. S. GEOLOGICAL SURVEY 



WATER-SUPPLY PAPER 33R PLATE IX 




A. TRAVERTINE RIDGES NEAR BRIDGEPORT, MONO COUNTY. 




^^S .*^"-^ '^'f^'f- -v.-» - '■'% 



£. CARBONATE DEPOSIT BESIDE INDIAN CREEK, PLUMAS COUNTY. 



HOT SPRINGS. 



135 



lowing analysis shows that it is rather strongly ])rimary alkaline and 
saline. 

Analif^s of water from spring from crevice in travertine ridge. Hot Springs near Bridgeport, 

Mono County, Cal. 

[Analyst and authority, F. M. Eaton (1910). Constituents are in parts per million,] 



Temperature 

Properties of reaction: 

Primary salinity 

Secondary salinity 

Tertiary salinity 

Primary alkaliiiity 

Secondary alkalinity 

Tertiary alkalinity 

Constituents 

Sodium (Na) 

Potassium (K) 

Calcium (Ca) 

Magnesium (Mg) 

Iron(Fe) 

Aluminum (Al) 

Sulphate (SO4) 

Chloride (CI) 

Carbonate (CO3) 

Silica (Si02) 

Carbon dioxide (COj) 



04° C. (148' F.) 

48 



44 
8 
6 



By 

weight. 



Reacting 
values. 



1,109 
35 
•50 
19 



9.39 
214 

844 
89 



48.22 

.90 

3.01 

1.56 

.06 

19.55 
6.04 

28.14 
2.96 



3,310.8 



Present. 



Present. 



Although the water is strongly mineralized, water from one of the 
springs, wliich is said to contain 1 pound of solid matter in 17 gallons 
(about 7,000 parts per million), was used without causing serious 
trouble in the boiler of a hoisting engine at the quarry, by injecting 
about a gill of kerosene a day. 

Tlie ridges seem to have been formed by deposition along the sides 
of fissures, continuing until the opening was reduced to a mere crack 
or was closed entirely. 

The lava from which the two groups of springs near Bridgeport 
rise possibly gives the water its thermal and also its chemical char- 
acter. In regard to the latter character, the association of lava with 
hot springs that deposit lime carbonate is here again to be noted. 

WARM SPRINGS BETWEEN BRIDGEPORT AND BODIE (MONO 5). 

In the mountainous region between Bridgeport and Bodie ther- 
mal water rises in Warm Spring Flat, but no information is at hand 
concerning either its temperature or its discharge. The springs are 
thought to be relatively small and unimportant, however, and they 
are probably used only as watering places for range stock. 

Another warm spring issues near Mormon Creek, 1^ miles south- 
east of Warm Spring Flat. It is worthy of note that Fales Hot 
Springs (Mono 1), the hot springs near Bridgeport (Mono 3), and 
the springs in Warm Spring Flat and on Mormon Creek he in a direct 



136 SPRINGS OP CALIFORNIA. 

line that, if extended southeastward, would pass 8 miles north of the 
Mono Basin Warm Springs (Mono 8, p. 145). 

BENTON HOT SPRING (MONO 12). 

About 300 yards northwest of the store and post office at Benton, at 
the base of slopes that border an area of meadowland, is a spring that 
forms a shallow pool approximately 10 feet in diameter in which the 
water has an observed temperature of 135°.^ It has furnished a sup- 
ply of water for the town for domestic and irrigation uses since the 
sixties, and in the early days it also furnished power for a small stamp 
mill. Its discharge is approximately 400 gallons a minute. The 
water as it rises effervesces with a gas that is probably carbon dioxide. 
A small amount of an efflorescent salt — probably Epsom salt — forms 
near the margin of the pool. A quantitative analysis of the water 
is not at hand, but the total amount of solids in solution has been given 
as 260 parts per million.^ 

The surrounding region is mainly granitic, but the slopes immedi- 
ately north of the springs are of white volcanic ash or tuff that con- 
tains rounded lava gravel. This material lies nearly horizontal on 
weathered gray granite. In a canyon half a mile west of the spring 
are numerous bands of dark basaltic material, up to 2 feet in thick- 
ness, that are, however, considered to be inclusions and not intru- 
sions in the granite. The intimate association of lava with the gran- 
ite, both of the tuff and the inclusions, suggests that here again the 
lava offers an explanation for the existence of the spring and also for 
the quantities of carbon dioxide that rise with the water. 

WARM SPRING IN SALINE VALLEY (INYO 12). 

There are a iew thermal springs of minor importance in the desert 
region of eastern California. One of these springs is at the northeast 
side of Saline Valley, about 25 miles in a direct line east of Independ- 
ence. It yields a small flow, and its water is not of high temperature. 
There are several cool springs a short distance westward from it and 
also to the southeast that form watering places in this part of the 
desert. 

WARM SPRING IN PANAMINT VALLEY (INYO 29). 

About 4 miles north of BaUarat, on the eastern edge of Panamint 
Valley, is a spring similar to ihe one in Saline Valley. Its water is 
tepid and is noticeably sulphureted, and its yield is only about 40 
barrels a day (1 gallon a minute). It forms a small watering place 
on a road leading northward from BaUarat. 

1 A temperature of 138° was recorded in this spring in 1876 by the Wheeler Survey (U. S. Geog. Surveys 
W. 100th Mer., 1876, p. 196), where it is stated that the temperature is considered to vary 5°. In the 
Eighth Report of the California State Mining Bureau, 1888, pp. 356 and 357, temperatures of 135.5° in 1870 
and 134.6° in 1888 are recorded. 

2 Wheeler, G. M., U. S. Geog. Surveys W. 100th Mer., 187G, p. 196. 



HOT SPRINGS. 137 

HOT SPRINGS NEAR TECOPA (INYO 35). 

About 2 miles north of Tccopa railroad station two hot springs 
issue on alkaline slopes that border the eastern side of an alkaline 
marsh along Amargosa River. The springs rise in pits that have been 
dug about 10 yards apart, and their combined flow is about 225 gal- 
lons a minute. Tlie observed temperatures were 108° and 109°. 
Near the springs are heavy alkaline deposits of soda and common 
salt, and the water tastes noticeably, though not disagreeably, of the 
alkalies. In 1908 the water was piped to a railroad watering tank 
half a mile westward. It has also been used to some extent for bath- 
ing at a pool near the springs. 

The water issues at the southwest base of a steep hill of qnartzite 
that dips about 15° NE. The structure suggests that the liill forms 
part of a range that has been faulted and tilted in the manner char- 
acteristic of the Basin Ranges and that the springs rise along the 
zone of fracture. Other warm seepages rise in marsh land a mile 
southward and probably have the same origin. 

SARATOGA SPRINGS (SAN BERNARDINO 3). 

Saratoga Springs, situated at the eastern border of south Death 
Valley, at the base of the Black Mountains, have long been known to 
desert travelers, but they are hidden from view at a distance by a 
narrow rocky spur on the south and by sand dunes on the north and 
west. As there is plenty of water at the place and a considerable 
area overgrown with marsh grass, prospectors usually stop here 
for a few days to allow their animals to rest after excursions into the 
surrounding mountains, and in 1908 a stone cabin and other build- 
ings were being erected by parties who had mining claims in the 
mountains near by. 

The principal spring forms a pool about 25 by 35 feet in diameter 
and 3 feet deep, in whose sandy bottom the water can be seen rising 
at a dozen or more places. The temperature of the w^ater is about 
82°, and the pool is inhabited by many small fish, which have been 
identified by Prof. J. O. Snyder as Cyprinodon macularius, the species 
that live in other desert springs of similar character. At three 
other points along the base of the hills, 100 to 250 yards northeast- 
ward from the main spring, water has been obtained by excavating 
into the slopes. An area of marsh grass, tules, and open water ex- 
tends 600 yards northward from the springs, but on account of the 
great evaporation the area of open water varies much with the sea- 
son. The water tastes distinctly of alkali, but it has formed no 
noticeable alkaline deposits. 

The mountains to the northeast consist of hard, altered limestones 
and sandstones that dip 25°-50° E. Some granitic rock is also 



138 SPEIISrGS OF CALIFORNIA, 

exposed at places near the base of the slopes. The small ridge at 
whose end the main spring rises is of dioritic material. 

Like many other ranges of this region, the Black Mountains appear 
to be a faulted block that dips eastward. Saratoga Springs rise at a 
point along this block where the intrusive dioritic rock has possibly- 
produced conditions that permit the escape of water from a moderate 
depth. It does not seem probable that this spring is supplied either 
by water from the sink of Amargosa River or by deep alluvial water 
that may here be brought to the surface, for the surface slope, the 
temperature of the water, and its freshness compared with the water 
of Amargosa River do not favor either source. 

MORGAN HOT SPRESTOS (TEHAMA 2). 

In the neighborhood of Lassen Peak, in the northeastern part of the 
State, there are some remarkable hot springs, whose positions with 
respect to each other and the peak are shown on Plate XI ^ (p. 140). 
The best-known gi'oup is at the southern base of the mountain on the 
Morgan ranch, where about 25 springs and pools are scattered for a 
distance of 600 yards in a meadow along Mill Creek. Most of them 
are quiet pools of small flow, less than 5 feet in diameter and relatively 
shallow. A number of them contain thick algous growths, and 
several deposit native sulphur. Others rise in areas where hard 
deposits of sihceous and of calcareous materials have formed. Three 
or four springs steam and sputter from vents on the banks of the 
creek. One of the northernmost of these springs seems to have a 
true geyser action, for it issues in a shallow basin 3 feet in diameter 
in which the water is said to come to a state of vigorous ebullition 
and then to subside about once a day. During a period of 41 hours 
the condition of this spring was noted five times as follows: At the 
beginning of the period, in active ebulhtion, discharge about 15 
gallons a minute, temperature 200° + ; two hours later quiet, no 
overflow, temperature 187°; at 16 hours and at 25 hours later in 
active ebuUition, overflowing; at 41 hours, quietly overflowing, about 
5 gallons a minute. 

The place has been a camping resort for a number of years. In 
1910 there were log bathhouses at three springs, a small shed over 
another pool, and a vapor bathhouse over a vent at the creek edge. 

An analysis (tabulated on p. 142), of water from one of two pools, 
about 3 feet in diameter, in an area of hard siliceous deposit 45 yards 
west of the creek edge and 50 yards north of the eastern log bath- 

1 The descriptions of hot springs in the Lassen Peak region apply to conditions during 1909-10. The 
conditions vary from time to time and possibly were considerably changed by the renewed activity of 
the peak ia 1914. The mountain, which had been considered an extinct volcano, broke forth on May 30, 
1914, in eruptions that appear to have been volcanic, not geyser-like, and at intervals vapors, volcanic 
dust, and stones were cast out from two small craters developed near the summit. 



HOT SPRINGS. 189 

house, shows that it is decidedly salty. The high content of silica 
shown by the analysis is also worthy of note. A few other hot springs, 
notably AiTOwhead Hot Springs (p. 32), contain approxmiately as 
much silica, but the siliceous deposit at the Morgan sprmgs is 
thought to be the largest spring deposit of this material in the State. 
In fact the only other hot spring locaUty where notable amounts of 
silica have been deposited is believed to be at Casa Diablo Hot 
Pool (p. 147). LeConte and Rismg mention the deposition of silica 
at Sulphm- Bank* (Lake 38) (p. 98), but it there takes place under- 
gi'ound and is not noticeable to the casual observer. 

It is possible that the water is magmatic and juvenile — that is, that 
it was originally contained in the underlying rock masses — and that 
it reaches the surface of the earth for the fu-st time in the springs. 
The sodium, chlorine, and also the silica may therefore be derived 
from the deep-seated rock magma or semifluid mass. Diller^ has 
shown, however, that a strait or arm of the ocean once occupied this 
area, which has since been uplifted and on which the mountain mass 
of Lassen Peak has been built up, and that the Chico formation, 
consisting of marme sediments, which outcrops 20 miles west and 
southwest of Morgan Hot Springs,^ probably und-erlies the lava of 
Lassen Peak. The suggestion, based only on the chemical character 
of the water and the geologic structure that has been worked out by 
Diller, is therefore offered that the Chico beds furnish the salme con- 
stituents of the water at Morgan Hot Sprmgs. The solvent action 
of this hot, salme water as it rises through the overlying lavas may 
accomit for the imusually high content of silica in the water, although 
literature concerning the solvent power of hot saline solutions on 
silicates has not been found. 

The slopes on each side of the meadow at Morgan Hot Sprmgs are 
covered with pyroxene andesite of Miocene or Pliocene age,* but a 
cemented conglomerate is exposed along the creek in the meadow 
where the sprmgs rise. The cementmg material is siliceous and 
probably has been deposited by the hot water. 

Three-fourths of a mile northeastward, on a branch of Mill Creek, 
is another hot spring over which a batliliouse containing several 
compartments has been built. This spring also rises in a hard con- 
glomerate similar to that at the springs m the meadow. 

1 LeConte, Joseph, and Rising, W. B., The phenomena of metalliferous vein formation now in progress 
at Sulphur Bank, Cal.: Am. Jour. Sci.,3dser., vol. 24, p. 33, 1882. 

2 Diller, J. S., Geology of the Lassen Peak district: U. S. Geol. Survey Eighth Ann. Kept., pt. 1, p. 413, 
i889; Tertiary revolution in the topography of the Pacifie Coast: U. S. Geol. Survey Fourteenth Ann. 
Kept., pt. 2, p. 423, 1894. 

3 Diller, J. S., U. S. Geol. Survey Geol. Atlas, Lassen Peak folio (No. 15), p. 1, 1895. 
< Diller, J. S., idem, areal geology sheet. 



140 SPKINGS OF CALIFORNIA. 

BUMPASS HOT SPRINGS (SHASTA 16). 

Bumpass Hot Springs (PL X, C) are situated on the side of Lassen 
Peak, about .9 miles by trail northward from Morgan Hot Springs 
(Tehama2,p. 138). Theyconsistof numerous pools of hot water, some 
of them in vigorous ebullition and rendered turbid by mud, and others 
less active but turbid with sulphur in suspension. Some pools con- 
tain acid or astringent water which is usually turbid with clay. The 
analysis given on page 142, with analyses of water from Devils Kitchen 
and Morgan Hot Springs, shows the composition of water from one 
of the principal springs, which is noticeably acid and sulphureted. 

The position of the vents and the activity of the discharge change 
from time to time and seem to be influenced to a large extent by the 
surface supply of water, for the springs themselves yield a relatively 
small amount. In November, 1909, the stream running from them, 
which is a branch of Mill Creek, carried perhaps 200 gallons a minute 
at a time when the adjacent slopes were covered with snow. In the 
following July it carried perhaps half as much, though melting 
patches of snow still covered parts of the near-by slopes. On the 
earlier date there was a pond 20 yards across, at whose edge was a 
large vent, from which muddy water was being thrown to a height 
of 10 feet, but in the summer this pond was nearly drained and the 
active spring had subsided to a sputtering pool. 

The area covered by the springs and vents of Bumpass Hot 
Springs — or Bumpass Hell, as it is locally called — is only about 200 
yards long and 100 yards wide, but the rock for some distance 
surrounding the active area has been altered to a white, siliceous 
material by acid water and solfataric vapors. About 300 yards 
downstream from the main area there is an area perhaps 50 yards in 
diameter where also the rock has been greatly altered. When visited 
vapor still escaped from numerous small vents, and needles of sulphur 
crystallized at their orifices, but no water was flowing from them. 

The locality has been mapped geologically by Diller ^ as a small 
area of basaltic lava at the lower border of dacite that overlies 
pyroxene andesite. The small basaltic area appears to have been 
intruded through these earlier lavas that form the greater part of 
Lassen Peak. 

In 1910 the springs were occasionally visited as a natural curiosity, 
but the mineralized waters were not used for bathing or for other 
purposes. The Lassen Peak region is rapidly becoming a summer 
vacation ground, however, both because of the excellent fishing in its 
numerous streams and small lakes and because of its scenic features, 
and Bumpass Hot Springs will probably become a favorite objective 

1 DiUer, J. S., U. S. Geol. Survey Geol. Atlas, Lassen Peak folio (No. 15), 1895. 



U. S. GEOLOGICAL SURVEY 



WATER-SUPPLY PAPER 338 PLATE X 



|:;-^^^5^. .-,. 




i 




A. THE GEYSERS, SONOMA COUNTY. 




B. CASA DIABLO HOT SPRINGS, .ViOiJO COUNTY. 




C. BUMPASS HOT SPRINGS, SHASTA COUNTY. 



U. S. GEOLOC 
GEORGE OTIS S 



121° 45' 



121-4:5' 



From Lassen Peak < 
U. S. Geological 



U. S. GEOLOGICAL SURVEY 
GEORGE OTIS SMITH, DIRECTOR 



WATER-SUPPLY PAPER 338 PLATE XI 




MAP OF LASSEN PEAK REGION, CALIFORNIA 



Contour iiitei*val 200 Petl 

DattimiJtmean Sea.7e-Te7 

1914 



HOT SPRINGS, 141 

point for outing parties from camps on the lower slopes. (See PI. 
XI.) As these springs are only 3 miles from the craters formed in 
Jime, 1914, their character probably has also been changed. 

SOUPAN HOT SPRINGS (SHASTA 15). 

Soupan Hot Springs are about 2^ miles directly west of Bumpass 
Hot Springs, on the western side of the main canyon of Mill Creek, 
which is separated from the Bumpass springs by a divide only about 
100 feet high. The springs jdeld a small amount of hot water similar 
in character to that of the Bumpass springs but are of interest 
chiefly because of the neighboring deposits of sulphur. These 
deposits were at one time prospected and the pits are still locally 
kno\\^l as the ' 'sulphur works," but they were never worked on a 
commercial scale and have long been abandoned. 

Soupan Hot Springs, like the Bumpass springs, are in an area of 
altered lava, but apparently only the older Neocene lava of Lassen 
Peak is exposed. A carbonated spring (Shasta 14, p. 227) that issues 
about H miles north of Soupan Hot Springs, is of geologic interest, 
for its presence indicates that much of the bubbling at the hot 
springs of the vicinity may be due to carbon dioxide instead of steam. 

DEVILS KITCHEN (PLUMAS 1). 

At the head of Hot Spring Valley is an area called the Devils 
Kitchen in which the lava has been extensively altered by solf ataric 
action in a way similar to that observed at the Bumpass and the 
Soupan springs. The Kitchen differs somewhat in position from 
these other hot springs, however, as it is in the bottom of the stream 
canyon and is bordered by cliff -like walls. Numerous bubbling 
and sputtering pools form "paint pots" and mud cones over the 
bottom, which is about 200 yards across and is in many places floored 
by a treacherous crust that overlies scalding mud. Steam issues 
from many large vents around the border of the area, and in cool 
weather the clouds of vapor make an interesting and unusual sight. 
The analysis of water from a large pool near the center of the area 
shows that it is only moderately mineralized in regard to total con- 
tent, but the large proportion of silica, sulphate, and of tertiary 
salinity makes it a very unusual water. The wide differences in 
character shown by the following chemical analyses of the three 
hot springs in the Lassen Peak region are of special interest. 



142 



SPRINGS or CALIFOENIA. 



Analyses of ivater from Devils Kitchen, Plumas County; Bumpass Hot Springs, Shasta 
County; and Morgan Hot Springs,: Tehama County, Cal. 

[Analyst and authority F. M. Eaton, 1909-10. Constituents axe in parts per million.] 



Properties of reaction: 

Primary salinity 

Secondary salinity . . . 

Tertiary salinity 

Primary alkalinity. . 
Secondary alkalinity 
Tertiary alkalinity . 



36 
29 
35 


140 



Constituents. 



By 
weight. 



Reacting 
values. 



By 
weight. 



Reacting 
values. 



By 

weight. 



Reacting 
values. 



Sodium (Na) 

Potassium (K) 

Calcium (Ca) 

Magnesiimi (Mg). . 

Iron(Fe) 

Aluminum (Al). . . 

Hydrogen (H) 

Sulphate (SO4)..- 

Nitrate(N03) 

Chloride (CI) 

Carbonate (CO3). . 
Metaborate (BO2). 
Phosphate (PO4). 
Silica (Si02) 



20 
11 
11 
50 
10 
963 



1.80 

.25 

1.00 

.92 

.39 

5.57 

10.12 

20.05 



Trace. 






Trace. 

.00 

.00 

.00 

9.50 



16 
14 
8.9 
5.1 
1.4 
5.3 
.37 
141 

Trace. 

Trace. 





0.70 
.36 
.44 
.42 
.05 
.59 
.37 
2.93 

Trace. 

Trace. 
.00 



1,416, 
122 



Trace. 
2.2 



61.57 

3.12 

4.48 

Trace. 



2.12 



2,342 
25 
Present. 



66.05 

.83 

Present. 



1. Devils Kitchen springs. 

2. Bumpass Hot Springs. 

3. Morgan Hot Springs, the northwestern of two pools 75 yards northeast of log bathhouse. 

In 1910 the water from springs in Devils Kitchen had not been 
made use of, but as the place is easily accessible from Hot Springs 
Valley it was visited by camping parties as a place of scenic interest. 

DRAKE HOT SPRINGS (PLUMAS 4). 

Drake Hot Springs issue along the side of Hot Springs Valley about 
1-| miles east of Devils Kitchen. For many years the j)roperty has 
been a camping resort and within recent years accommodations for 
guests have been provided during the summer months. 

The springs are scattered for a distance of 100 yards or more, 
mainly along the slope on the south side of Warner Creek, but one 
of the principal springs, which yields about 3 gallons a minute of 
water 128° in temperature, issues from a seam in rock at the south 
edge of the creek. In 1910 a small bathhouse and a wooden tank 
that was used as a plunge bath were supplied mth hot water from 
three springs 40 or 50 yards south of the creek. These springs yield 
a total of perhaps 15 gallons a minute at temperatures of 123°, 146°, 
and 148°. The peculiar characteristic of this water is its appar- 
ently slight mineralization, for it has no noticeable taste and only 
a slight odor of hydrogen sulphide. At three or four places on 
the bank above the creek, however, axe deposits of lime carbonate, 



HOT SPKINGS. 143 

indicating that the water carries some carbon dioxide and calcium, 
but the quantity of calcium in the water is not sufficient to make it 
appreciably hard. 

TARTARUS LAKE (PLUMAS 5). 

About 1 mile east of south from Drake Hot Springs (Plumas 4, 
p. 142) lies a shallow, oval pond, approximately 175 yards long and 100 
yards wide, that is known as Tartarus Lake. An overflow channel 
leads northwestward from it, but in the summer of 1910 this channel 
carried no water. A number of mud pools or "paint pots" on its 
northern and northwestern border were in sluggish action, and at its 
southeastern end were sputtenng and steaming vents with temper- 
atures of 170°. Although the surface of the lake was apparently 
quiescent, the water was turbid and slightly yellow in color, proba- 
bly from sulphur in suspension. It was said that two years previous 
the lake was vigorously bubbling throughout nearly its whole extent. 
During the season of greatest run-off the lake receives the drainage 
from the surrounding slopes and then overflows, but it ordinarily 
contains only a small amount of water. The water, like that of sev- 
eral other hot springs in areas of solfataric action in the region, 
tastes astringent and probably contains an unusually large amount 
of aluminum and sulphate. 

The lake lies in a small depression surrounded by moderate slopes 
beside a trail that leads from Willow Lake northwestward to Drake 
Hot Springs. In several places close to the lake the lava of the 
Lassen Peak region has been altered to white siliceous material, 
but an area several yards ^vide on the western side of the lake con- 
sists largely of white and iron-stained kaolin. The locality presents 
features similar to those at Bumpass Hot Springs and Devils Kitchen, 
but the action of the springs, like that at Soupan Hot Springs, ap- 
pears to be much less vigorous. 

THE GEYSER (PLUMAS 6). 

In a ravine about 2^ miles southeast of Tartarus Lake there is an 
actively boiling pool locally kno\\Ti as The Geyser (PI. V, C, p. 50). 
A main pool, about 25 feet in diameter, is situated at the base of 
steep slopes, and in July, 1910, the water was continually thrown to 
a height of 1 to 3 feet from a vent in its northern part. From the 
main pool the water overflowed into another, somewhat smaller pool, 
in the center of which there was a distinct upward current and from 
which the overflow escajjed down the ravine. In the center of a 
third pool or basin about 10 yards south of the main pool there 
was also a distinct upward current, and from this pool a stream of 
2 or 3 gallons a minute overflowed. Although the main spring was 
in very active ebullition, it also discharged only 2 or 3 gallons a 



144 SPRINGS OF CALIFOENIA, 

minute, and nearly all its water apparently came from two hot springs 
in the bowlder-strewn drainage channel on the slope 10 or 15 yards 
northwest of it. The slope immediately north of the springs is 
altered to white siliceous material, but the water has no distinctly 
mineralized taste. 

It is said that during the seventies the main spring cast water to a 
height of 10 feet or more and was more truly geyser-like in action. 
Residents in the region say that its energy has been gradually di- 
minishing and has noticeably decreased within the last few years. 
Information is not at hand, however, regarding the influence of the 
seasons on its action or the extent to which its vent has been choked 
by rocks thrown into the pool. 

Lassen Peak and the country that surrounds it for a number of 
miles are composed of lavas of comparatively recent geologic age, 
being assigned to the Neocene epoch of geologic history. In at least 
one place, however, which is at Cinder Cone, there is evidence of an 
eruption that is believed to have taken place within two cen- 
turies.^ The existence of numerous hot springs in this region there- 
fore seems to be connected with the presence of the recent lava, and 
the water probably receives its heat from underlying masses of lava 
that have not yet cooled down to the normal temperature of the sur- 
rounding rocks at that depth. This condition is strongly indicated 
by the renewed activity of the peak in May and June, 1914. 

HOT SPRINGS ON MOUNT SHASTA (SISKIYOU 14). 

Vapor and small amounts of hot water rise at two localities near 
the summit of Mount Shasta. These localities are of relatively little 
importance as hot springs, but their presence at such an elevation 
and position is of geologic interest with respect to the mountain, 
which is a volcano that has become extinct within comparatively 
recent geologic time. The heat of the water, as at the springs near 
Lassen Peak, is probably derived from heated lava within the moun- 
tain. 

HOT SPRINGS ON PAOHA ISLAND (MONO 7). 

Along the eastern front of the Sierra there are other groups of hot 
springs whose existence seems to be closely related to lavas of recent 
geologic age. One of the northernmost of these groups is on the 
east side of Hot Spring Cove, on Paoha ^ Ipland in Mono Lake. The 
western part of the island is covered with lake sediments, but the 
eastern part is formed of black lava, and on its most southeastern point 
vapor and small amounts of hot water issue from numerous crevices. 

1 Diller, J. S., U. S. Geol. Survey Geol. Atlas, Lassep Peak folio (No. 15), p. 4, 1895. 

2 Because of the hot springs an Indian term (pa-6-ha) meaning "spirits of the mist" was applied to the 
island by Prof. I. C. Russell in The Quaternary history of Mono Valley, California: U. S. Geol. Survey 
Eighth Ann. Rept., pt. 1, p. 279, 1889. 



k 



HOT SPKINGS. 



145 



One tipring, which has a touii)oiatiiic ol" 17G° and cUschargOis about 15 
(gallons a mmuto, was observed close to the water's edge. It is 
wortliy of note tluit the maxiinuni teni])ei-atiire in the tliernial 
si)iings at this locality observetl by Russell ' at a time when the 
lake surface was several feet lower than it was in 1908, was 110°. 
Apparently the increased pressure (hie to a higher lake level lias re- 
sulted in higher temperature of the water. This hot water is compar- 
atively ])ure, and when^ it mingles witli the cool, strongly alkaline 
water of tlie lake the convection currents ])roduce an. oily appearance, 
^lucli va])or rises for a considerable (Hstance along the base of the 
lava bluffs that border this part of the island, and the oily appearance 
of tlie lake surface shows tluit considerable hot water rises beneath 
it. In 1908 the springs furnished a water supply for a goatherd who 
ranged his animals on the island. 

MONO BASIN WARM SPRINGS (MONO 8). 

In 1881 Russell visited Mono Basin Warm Springs, which then 
rose m Mono Lake a short distance from its eastern edge and were 
occasionally used for bathing. Springs also rise from tufa domes in 
the lake. The following anal3^ses are of a warm spring on the eastern 
shore and of a spring issuing from a tufa dome near Black Point, on 
the western shore : 

Analyses of tvater from springs in Mono Lake Basin. 

[Analyst, T. M. Chatard (1884). Authority, U. S. Geol. Survey Bull. 9. Constituents are in parts per 

million.] 



Temperature 

Properties of reaction: — 

Primary salinity 

Secondary salinit y 

Tertiary salinity 

Primary alkalinity 

Secondary alkalinity 

Tertiary alkalinity." 

Constituents. 

Sodium (Na) 

Potassium (K) 

Lithium (Li) 

Calcium (Ca) 

Magnesium (Mg) 

Aluminum ( Al) 

Sulphate (SO^) 

Chloride ((M) 

Silica (SiO;) 



-32°C.(80°-90°F.); 

36 


42 
22 
(?) 



(V) 



1, Spring on eastern shore of Mono Lake. 

2, Spring near Black Point, Mono Lake. 



By 
weight. 



612 

63 

Trace. 

59 

60 

LO 
313 
227 
122 



1,457 



Reacting 
values. 



26. 59 

1.61 

'I'race. 

2.94 

■ 4.97 

.11 

6.52 

6.41 

4.05 



By 

weight. 



51 

8.8 



41 
4.4 



Reacting 
values. 



2.23 
.23 



2.07 
.36 



1.14 
.41 
. 59 



' Russell, 1. C, op. eit., p. 288. 
wsp 338—15 10 



35657"= 



146 SPEINGS OF CALIFORNIA. 

The analyses show that the waters are of the same general primary- 
sahne and primary-alkaline type, though that of the warm spring is 
more concentrated and contains a less proportion of secondary bases 
than that of the spring near Black Point. The relatively greater 
proportion of sihca and the higher magnesium-calcium and chloride- 
sulphate ratios of the warm spring are also noteworthy. 

South of Mono Lake there is an area of prominent volcanic craters 
that are composed largely of fragmental material. These craters are 
considered to be of very recent geologic age. Their presence and the 
fact that the hot water on Paoha Island issues directly from lava 
furnish good evidence that the heat of the springs is derived from 
underlying lava that has not yet cooled to the normal temperature 
of the surrounding rocks. 

CAS A DIABLO HOT SPRINGS (MONO 16). 

In the southwestern part of Mono County, near the base of the 
Sierra, hot water rises at several localities. The principal group^ 
known as Casa Diablo Hot Springs (PL X, B, p. 140), is situated on 
lava slopes bordering Hot Creek, about 200 feet above open meadow 
land and at the base of steeper slopes of lava. One main spring here 
forms a pool about 15 feet in diameter, in which the water is in vio- 
lent ebullition and is thrown to a height of 12 to 18 inches. The dis- 
charge is only about 15 gallons a minute, however, so the vigorous 
action is probably due largely to steam or other gas. Near the edge 
of the pool a temperature of 194° was recorded, which is only about 
4° below the boiling point at this elevation (about 7,350 feet), and the 
water is probably at the boihng point in the center of the pool. The 
water is rendered very turbid by pink clay. Small amounts of vapor 
rise in half a dozen small pits that have been dug a few yards south 
of this pool. At a distance of 60 to 100 yards north of the main pool 
there are a dozen or more pools 2 or 3 feet in diameter in which ob- 
served temperatures range from 115° to 187°. They discharge from 
one-half gallon to 5 gallons a minute each, and the water forms a 
small marshy area, at the edge of which a small bathhouse has been 
erected. A log cabin has stood near by for a number of years, for the 
springs have long been visited by white people as well as by the 
Indians for rehef in rheumatic and kindred troubles. Other small hot 
vents about 50 to- 75 yards northeast of the bathhouse supply a shal- 
low pool that discharges perhaps 5 gallons a minute. A quarter of a 
mile northeast of these springs there is still another group which 
supplies a pool measuring about 20 by 60 yards that discharges 15 
gallons of scalding water a minute. In this pool the water rises 
mainly from a conical basin. A small pit in the bank near its margin 
forms a "paint pot" in which pink mud is kept in motion by bubbles 
of steam or other gas. In this material a temperature of 198° (proba- 
bly the boiling point) was recorded. 



HOT SPRINGS. 147 

At the base of liills a quarter of a mile northeastward is a shal- 
low circular basin in the volcanic soil and gravel. In 1908 no 
water or noticeable amount of vapor issued here, but at four 
places the ground was hot. An Indian 50 or 60 years old, who was 
met at the springs, volunteered the information that this basin was 
formerly more active, and he described in gi-aphic manner the rum- 
bling that years ago was heard here. The rumbling of the present 
springs is occasionally heard at a distance of several miles, especially 
during cold weather. 

CASA DIABLO HOT POOL (MONO 16). 

About 3^ miles east of Casa Diablo Hot Springs there is a shallow 
pool, measuring about 30 by 35 yards, which may be called Casa 
Diablo Hot Pool. In November, 1908, this pool was not over- 
flowing, though there was a small, well-defined outlet channel from 
it toward Hot Creek. Over nearly its entire bottom were numerous 
vents in which water bubbled and in several of which, near the margin, 
temperatures of 120° to 180° were recorded. Near the western bor- 
der of the pool there are small amounts of soda alkali and also a little 
alum, and along part of the overflow channel there is a hard deposit, 
apparently of sihca and lime carbonate, which also covers an area 
about 50 yards in diameter near the drainage channel. Its formation 
indicates that a portion of the bubbles that rise in the pool are of 
carbon dioxide rather than of steam. The pool is situated at the base 
of a small lava bluff that trends northw^ard along the hillside and that 
has the appearance of a small fault scarp, but it may be only a small 
persistent scarp of erosion. 

HOT SPRING NORTHEAST OF CASA DLA.BLO HOT SPRINGS (MONO 14). 

About 5 miles northeast of Casa Diablo Hot Springs there is a 
pool, apparently of considerable depth, in which the water has a 
scalding temperature and is mildly sulphureted. It is not so active 
as the more southern springs, though it is sunilar to them in character. 
Like the Casa Diablo Hot Springs and Hot Pool, it is situated at the 
eastern front of the Sierra, in an area covered by comparatively 
recent lava, and both its position and its activity suggest that, 
like the springs in the Lassen Peak region, its heat is derived mamly 
from underlying lava and that places for the surface escape of the 
water may be furnished by faulting. 

WARM SPRINGS IN LONG VALLEY (MONO 17). 

In Long Valley, 8 miles west of Owens River and about 7 miles 
south of east of Casa Diablo Springs, there are tw^o oblong pools 
a few feet apart and 40 feet long in which wann water rises and from 
which it flow^s to a shallow pond called Whitmore Tub. A maxi- 



148 SPRINGS OF CALIFORNIA. 

mum temperature of 100° was recorded in the pools, and the dis- 
charge measured was about 450 gallons a minute. The water rises 
quietly and has no distinct taste nor odor. Much dark-green algous 
growth lines the pools and the discharge channels, and small snails 
live in the water. 

The springs rise in a flat, salt-grass area about 100 j^ards south of 
the base of lava hills and 15 or 20 yards west of a 6-foot terrace- 
like bank that drops eastward toward the river. At two places 
along the edge of this bank springs that have about equal flows of 8 
gallons a minute issue with temperatures of 74° and 100°. The 
bank was not observed closely enough to be able to determine 
whether it is an old bank of Owens River or a small fault scarp. 
Like the Casa Diablo Springs, however, the position of the warm 
springs in a region of comparatively recent volcanic activity, where 
there has also been considerable minor faulting, affords suggestive 
evidence of the cause of their thermal character. Other similar 
springs rise about 3 miles farther north m the valley and form a 
small meadow. 

HOT SPRING SOUTH OF BISHOP (INYO 1). 

At the base of the Sierra about 8 miles south of Bishop a spring 
of considerable flow that is utilized for domestic supply and also for 
dipping sheep has a temperature of about 130°.^ Like the sprmgs 
farther north, in Long Valley, its water has no distinctive taste nor 
odor and is probably mineralized in only small amount. 

Volcanic rocks are present a few miles north of Bishop, and lava 
cones border the valley several miles south of the spring; but its 
water issues from granitic rocks, and the unusually high temperature 
seems more probably to be caused by rising from a considerable 
depth along a fault zone than by contact with masses of lava that 
have not yet cooled. 

WARM SPRING NEAR LITTLE LAKE (INYO 32). 

A small amount of lukewarm, odorless water issues in a spring 
about 300 yards from Little Lake and near the base of a lava bluff 
25 or 30 feet high. The spring has not been developed nor used to 
any extent during recent years and is known only locally. Perhaps 
the chief point of interest concernmg it is its position with respect 
to the lava bluff. The primary alkaline and saline character of the 
water is shown by the following early analysis: 

1 Reported by Adolph Knopf. 



HOT Si'KINGS. 



149 



Attrilysis of iratrr/roni War ni Spring near Little Luke, Inyo County, Cat. 
[Aiiulysl, Osciir Loow ^isyti). Authority, Wheeler report. Constituents are in parts per million.) 



Proper! ies of reaction: 

Primary salinity 

Secondary salinity 

Tert iury salinit y 

Primary alkalinity 

SeeonciaiN' alkalinity 

Tertiary alkalinity 

ToiLstituents 

Sodium (Na) 

Potassium ( K) 

Calcium (Ca) 

Magnesium (Mg) 

Sulphate (SO4) 

Chloride (CI) 

Carbonate (CO3) 

SUica (Si02) 




COSO HOT SPRINGS (INYO 31). 

Near the southwest corner of Inyo County there is a group of hot 
springs that are especially remarkable because of the acid character 
of their water. They have long been known as Coso Hot Springs, 
as they are on the eastern slope of the Coso range of niountams. The 
main group is about 12 miles east of Haiwee railroad station, and is 
beside a road that leads eastward to Coso and other mining camps. 
The rocks of the region are largely granitic, but this material is 
covered in some places by lava and by lava craters of a recent geo- 
logic period of eruption. 

At the principal spring, which is in granitic material, in a pit about 
50 by 100 feet in diameter and 10 feet deep, vapor and hot, sour 
water rise through a wliite mud that is apparently formed by the de- 
composition from the rock. In summer the water in this pit is low, 
but in winter, as a result of increased condensation and decreased 
evaporation due to cooler weather, it is nearly half full. 

The following analyses of the water show that it contains unusually 
large amounts of sulphate and of iron, aluminum, and silica. The 
most remarkable feature, however, is the high tertiary saUnity. The 
discordance of the two analyses is apparently due, in part at least, 
to a change in the character of the water. In connection with the 
large iron and sulphate content it is of interest to note that minute 
crystals, apparently of pyrite (iron sulpliide), collect as a fihn on the 
water and also form on the clay at the side of the pool. 



150 



SPEINGS OF CALIFORNIA. 



Analyses of water from Coso Hot Springs, Inyo County, Cal. 
[Constituents are in parts per million.] 



Properties of reaction: 

Primary salinity 

Secondary salinit.v . . 

Tertiary salinity 

Primary alkalinity. . 
Secondary alkalinitj' 
Tertiary alkalinity . . 



(?) 



Constituents. 



By 

weight. 



Sodium (Na) 

Potassium (K) 

Litliium (Li) 

Ammonium (NH4)- 

Calcium(Ca) 

Magnpsium (Mg). . . 

Iron(Fe) 

Aluminum (Al) 

Hydrogen (H) 

Sulphate (SO4) 

Nitrate (NO3) 

Chloride (CI) 

Carbonate (CO3) . . . 
Metahorate ( B O 2) . . 
Phosphate (PO4)... 
Silica(:Si02) 



49 

11 

Trace. 

Trace. 

45 

2.4 

122 

201 

16 

2,30s 

Trace. 

Trace. 





Trace. 



2, 7.54. 4 



Reacting 
values. 



By 

weight. 



2.13 

.29 

Trace. 

Trace. 

2.25 

.20 

4.98 

22.22 

15. 98 

48.05 

Trace. 

Trace. 

.00 



Trace. 



59 

34 

83 

56 

12 

1,400 



40 





Trace. 

411 



Reacting 
values. 



3.52 
.31 



2.84 

2.80 

2.97 

6.20 

11.67 

29.18 

.00 

1.13 

.00 

.00 

Trace. 

13.59 



1. Mainspring. Analyst, Oscar Loew (1870). Authority, Wheeler report. 

2. Mainspring. Analyst and authority, F. M. Eaton (1910). 

The place has become a camping resort for people afflicted with 
rheumatism, which is said to be relieved by baths in the hot mud. 
Bathing pits are dug in the cooler mud near the spring and the 
material is worked up to the desired consistency. Close to the main 
spring is an area of steam vents, about 25 by 50 yards across, which 
contains several pools that furnish clear water for washing and cook- 
ing. Tliis area also furnishes sufficient heat for cooking, kettles 
containing food being placed in shallow pits, covered with sacks, and 
allowed to remain until the food is done. 

Another area of hot vapors and mud in a ravine northwest of the 
main spring has been filed on as a placer claim for mining medicinal 
mud. The material at this place is somewhat finer in texture than 
that at the main spring. 

VAPOR VENTS WEST OF COSO HOT SPRINGS (INYO 30). 

Along the branches of a ravine 3 miles west of Coso Hot Springs 
there is an area several acres in extent in which much vapor issues 
and the ground is impregnated with sulphur and alum, but in 1908 
no water was flowing. A temperature of 203°, which is probably 
the boiling point at this elevation (about 4,300 feet), was recorded in 
the vapor vents. These vents are in an area of lava where there are 



HOT SPRINGS. 



151 



a iiiimbor of small volcanic craters, and tlio surface is partly covered 
with fragments of pumice and obsidian. At the vapor vents the rock 
has been extensively altered by solfataric action and reduced to a 
siliceous sinter, but a mud similar to that at the Coso Springs was not 
observed. This difference is probably due partly to the fact that 
there is not sufficient water at the vapor vents to form a mud, and 
partly because they issue through lava, which does not become knolin- 
ized as readily as does the granitic rock at Coso Hot ^Springs. 

SUMMARY OF HOT SPRINGS. 

The foregoing descriptions, comprising 149 springs or groups of 
springs, include 9 resorts at which there are no natural springs, so 
that the total number of hot-spring groups is 140. As several springs 
that have been described separately may be considered geographically 
to form only one group they have been gathered in the following list 
into 98 general localities, which have been arranged (1) according to 
the absence or presence of a notable spring deposit; (2) according to 
the absence or presence of lava near by, and (3) according to the char- 
acter of the material from which the water issues, this arrangement 
having been adopted in order to show clearly the formation of depos- 
its by hot springs, the relation of hot waters to lava areas, and their 
general geologic features. 

Ilot-spring localities. 
A. No notable deposits (88 localities). 

I. No lava nearby • 



1. 



alluvial 



Arrowhead Hot Springs. 
Waterman Hot Springs. 
Harlem Hot Spring (in 
gravel). 

2. Warm spring in Lytle Canyon. 

3. Warm spring at Baldwin Lake. 

4. Eden Hot Springs. 

San Jacinto Hot Springs. 
Ritehey Hot Springs. 

5. Pilares Hot Spring (in alluvium). 

6. Palm Springs. 

7. Glen Ivy Hot Spring. 
Elsinore Hot Springs (in alluvium). 
Bundys Elsinore Hot Spring (in allu- 
vium). 

Murrieta Hot Springs (in gravel). 

Warner Hot Springs. 

Agua Caliente Springs (San Diego 

County). 
Agua Tibia Springs. 

13. Deluz Warm Springs. 

14. San Juan Capistrano Hot Springs. 



In granitic rocks. 

15. California Hot Springs. 



8. 



9. 
10. 
11. 

12. 



16. Hot springs near Kernville. 

17. Neills Hot Spring (in alhunum). 

18. Clear Creek Hot Springs. 
Delonegha Springs. 
Democrat Springs. 

19. Williams Hot Springs. 

20. Paradise Springs. 

21. Blaney Meadows Hot Springs. 

22. Lower springs on South Fork of San 

Joaquin River. 

23. Hot springs at head of Fish Valley. 

24. Hot springs on North Fork of Little 

Sur River. 

25. Tassajara Hot Springs. 

26. Sespe Hot Springs. 

27. Warm springs in Elizabeth Lake 

canyon. 

28. Kruger Spring (in alluvium in rei^'ion 

of ancient effusives). 

29. Hot spring south of Bishop. 

30. Warm spring in Saline Valley. 



152 



SPRINGS OF CALIFOENIA. 



In comparatively unaltered sedimentary rocks. 



1. Fairview Hot Spring (in alluvium). 

2. Paraiso Hot Springs. 

3. Vickers Hot Springs. 
Stingleys Hot Springs. 
Matilija Hot Springs. 
Wheelers Hot Springs. 

4. Montecito Hot Springs. 

5. San Marcos Hot Springs. 

6. Las Cruces Hot Springs. 

7. Newsoms Arroyo Grande Warm 

Spring. 



8. Pecho Hot Springs. 

9. Paso Bobles Mud Bath Springs (in 

alluvium). 
Santa Ysabel Springs. 

10. Cameta Warm Spring. 

11. Fresno Hot Springs. 

12. Gilroy Hot Spring. 

13. Warm Springs (Alameda County). 

14. Byron Hot Springs (in alluvium). 



1. Slates Hot Springs. 

2. Dolans Hot Spring. 

3. Mercey Hot Springs. 

4. Rocky Point Spring (on the beach) 

5. Skaggs Hot Springs. 

6. Hoods Hot Springs. 

7. Orrs Hot Springs. 

8. The Geysers (Sonoma County). 

Little Geysers. 

9. Anderson Springs. 
Castle Hot Springs. 

10. Harbin Springs. 

II. Lava near by. 
In granitic rocks. 



mining 



In altered sedimentary rocks. 

11. Wilbur Hot Springs. 
Jones Hot Spring. 
Hot springs on Manzanita 

property. 
Blancks Hot Springs. 
Hot Springs at Elgin mine. 

12. Crab tree Springs. 

13. Warm spring in Panamint Valley. 

14. Hot springs near Tecopa. 

15. Saratoga Springs (intrusive rock near 

by). 



1. Jacumba Springs. 

2. Brockway Hot Springs. 



3. Coso Hot Springs. 



In altered sedimentary rocks. 



1. Gordon Hot Spring. 

Howard Springs (in serpentine). 
Seigler Springs. 



2. Bassett Hot Spring (in tuffaceous 
sandstone). 
Stonebreaker Hot Springs (in tuffa- 
ceous sandstone). 



In lava. 



1. Point Arena Hot Springs. 

2. Hot springs at Sulphur Bank (car- 

bonated). 

3. Warm springs of State Home at Eld- 

ridge. 

4. Los Guilicos Warm Springs. 
Warm springs on McEwan ranch . 

5. Mark West Warm Springs. 

6. Big Bend Hot Springs. 
Hot springs on Kosk Creek. 



7. Hot springs in Little Hot Spring 

Valley. 

8. Hot Springs on Hot Creek. 

Warm spring in Warm Spring Valley. 
Warm springs near Rattlesnake Creek. 
Warm springs near Canyon Creek. 

9. Hot springs on Bidwell Creek. 

10. Campbell Hot Springs. 

11. Warm springs between Bridgeport 

and Bodie. 



HOT SPRINGS. 



153 



111 l:iv:i - ('ontinuo(l. 



12. Benton Hot Sj)ring ((•ar})oiiate(l) 

13. lUiiiipass Hot Springs. 
Soupan Hot Springs. 
Devils Kitchen. 
Tartarus Lake. 



The Geyser (Plumas County V 

14. Hot springs on Mount Shasta. 

15. Hot springs on Paoha Island. 

16. Warm spring near Little Lake. 
Vapor vents west of ( 'oso Hot Springs. 



In alluvium. 



1. Mud Volcanoes. 

2. Calistoga Hot Springs. 

3. Kellys Hot Spring. 

4. Klamath Hot Springs. 

5. Hot springs near soutliM-est side of 

Upper Lake. 
Hot springs on (>ast side nf Surprise 

Valley. 
Hot springs at east border ot" Surprise 

Valley. 
Hot spring near east side (if Middle 

Lake. 



Hot sjirings near west side of Lower 

Lake. 
Hot springs near southwest .sid<' of 

Lower Lake. 
Warni springs at south end of Surprise 

Valley. • 
Boyd Spring. 

6. Marble Hot Wells (natural spring 

near by). 

7. Mono Basin Warm Springs. 

8. Warm springs in Long Valley. 



B. Notable deposits (10 localities). 

I. No lava near by. 

In granitic rocks. 



1. Jordan Hot Springs (calcareous de- 
posit). 



2. Buckeye Hot Springs (calcareous d« 
posit). 



II. Lava near by. 

In granitic rocks. 

1. Reds Meadows Hot Springs (calca- I 2. Grovers Hot Springs (calcareous de- 



reous deposit. 



posit). 



In lava. 



L Fales Hot Springs (calcareous de- 
posit). 

2. Warm springs near Bridgeport (cal- 

careous deposit). 
Hot springs near Bridgeport (calca- 
reous deposit). 

3. Morgan Hot Springs (siliceous and 

calcareous deposit). 

4. Drake Hot Springs (calcareous de- 

posit). 

In alluA'ium 



5. Casa Diablo Hot Springs (siliceous 
and calcareous deposit). 

('asa Diablo Hot Pool (siliceous and 
calcareous deposit). 

Hot spring northeast of Casa Diablo 
Hot Springs (no deposit, but con- 
sidered with the Casa Diablo 
group). 



1. Shaffer Hot Springs (calcareous de- 
posit). 
Amedee Hot Springs (calcareous de- 
posit). 



Ilighrock Spring (in alluvium at bor- 
der of lava, calcareous deposit). 



154 SPBIJSTGS OP CALIPOElSriA. 

In a general way the list shows the character of the rocks at the 
various hot-spring localities, although, as in other groupings, the 
springs can not be rigidly classified in this respect. The number of 
locaUties is seen to be about the same in regions of granitic rocks, of 
sediments (including the unaltered and the altered rocks), and of 
lavas (including those issuing from alluvium near lava), being respec- 
tively 36, 32, and 30. If any significance can be attached to this 
fact, it indicates that the presence of thermal springs is due in most 
places to structural conditions in which the character of the rocks is 
not an important factor. It apparently emphasizes the evidence 
shown by the faults on the map (PL III, in pocket), that the ex- 
istence of the thermal springs is due chiefly to crustal movements. 
Exception must be made, however, of a few thermal springs whose 
heat appears to be derived from lava that has not yet cooled to a 
normal temperature. 

There are notable deposits at 10 hot-spring localities. At 2 of 
these, Morgan Hot Springs and Casa Diablo Hot Springs, the deposit 
is in large part siHceous and the silica seems probably to be derived 
from the lava; at the other 8 there are notable deposits of lime 
carbonate, and 6 of these are closely associated with lava. At 
1 of the 2 remaining localities — Jordan Hot Springs — lava on the 
slopes to the north may possibly be in some way related to the 
deposit at the springs. Buckeye Hot Spring, the last of the 8, is 
only about 6 miles west of the springs near Bridgeport at which there 
are extensive lime carbonate deposits in a lava area, and there may 
be lava on the slopes near the Buckeye Spring, though it was not 
observed. The springs at Sulphur Bank, in Lake County, and Ben- 
ton Hot Spring, in Mono County, are the only hot, notably carbon- 
ated springs observed that do not form deposits of considerable size. 

The fact that most of the hot springs that issue in lava areas con- 
tain an excess of carbon dioxide and considerable sodium and mag- 
nesium with lesser amounts of calcium, suggests that the sodium 
and magnesium tend to deprive the calcium of bicarbonate and cause 
its deposition as hme carbonate. Thus the presence of notable 
amounts of carbon dioxide, derived presumably from the lava, and of 
the primary alkaHes sodium and magnesium, apparently causes the 
deposition of the calcium present in the form of carbonate. The 
same fact seems also to be shown by the cool carbonated springs at 
which there are notable deposits, as is indicated by the tabulated list 
on pages 252-253. It is significant that relatively few of the car- 
bonated springs that rise in sedimentary rocks form notable deposits, 
though some of them contain more calcium than do some of the hot 
springs that form extensive deposits. Most of the carbonated springs 
that do issue from sedimentary rocks and form deposits are noticeably 
thermal. 



CARBONATED SPRINGS. 155 

The conditions that were observed at the springs in CaliTornia well 
bear out the facts that have been recorded of springs elsewhere at 
which there are notable deposits. They show that the temperature 
of the water and its rate of cooling, the amount of carbon dioxide that 
is present, and the concentration of tlie solution — in other constitu- 
ents as well as calcium — all influence the deposition of calcium car- 
bonate. 

CARBONATED SPRINGS. 

NUMBER AND LOCATION. 

The number of carbonated springs — popularly known as soda 
springs — in California is larger than the number of hot springs, but 
few of the former class have been improved to greater extent than to 
form drinking springs at summer resorts. Most of them are of small 
flow, but they usually furnish good drinking waters. 

The carbonated springs (see PI. Ill, in pocket) are confined mainly 
to the coastal ranges north of San Francisco Bay and to a belt along 
the Cascade-Sierran uphft. The rocks of these regions have been 
briefly described (pp. 7-13) but are discussed in greater detail in 
connection A\ith the description of the springs. 

JACKSONS NAPA SODA SPRINGS (NAPA 12). 

One of the best known and most extensively developed mineral- 
spring resorts of the State is at Jacksons Napa Soda Springs, on the 
mountain side 650 feet above Napa Valley. The principal buildings 
here, which were erected during the eighties, are made of a volcanic 
tuff quarried near the springs. A bathhouse and a pa\'iHon are 
frame structures of more recent date. The property is open during 
the summer and provides accommodations for about 250 guests. 

In 1892 Anderson ^ mentioned 27 springs at this place, but in 1910 
only four were improved and made use of. Pagoda Spring, which 
rises in a hemispherical basin covered by a roof supported on stone 
])iUars, is the principal drinking spring, but when visited its visible 
overflow was only about one-eighth of a gallon a minute. The water 
is strongly carbonated and has deeply iron stained its basin. Lemon 
Spring, which is similar in character to the Pagoda Spring, issues 
in a stone-roofed basin at the side of the driveway, 25 or 30 yards 
below the Pagoda Spring. Two other springs rise in a stone house 
and are covered by tanks that collect the carbon dioxide that is 
given off. This gas is used to more heavily carbonate the water, 
which is piped to a large bottling house near by. The water has not 
])een extensively marketed east of the Pacific coast States, but has 
l)een shipped to Asiatic ports. 

1 Anderson, Winslow, Mineral sprinfts and health resorts of California, p. 202, 1892. 



156 



SPEINGS OF CALIFORNIA. 



The springs issue from slopes composed of tuff and rhyolitic lava. 
The following analyses show that the water of the two drinking 
springs is secondary alkaline in character and contains a relatively 
large proportion of magnesium and iron. 

Analyses of ivater from Jacksons Napa Soda Springs, Napa County, Cal. 
[Constituents are in parts per million.] 



Temperature 

Properties of reaction: 

Primary salinity 

Secondary salinity. . . 

Tertiary salinity 

Primary alkalinity . . . 
Secondary alkalinity . 
Tertiary alkalinity. . 



20° C. (6S°F.) 

14 



16 

70 

316 



20° C. (6S° F.) 

11 



14 
75 
14 



19° C. (67° F.) 





24 

68 
206 



Constituents. 



By 

weight. 



Sodium (Na) : 126 

Potassium (K) 1 Trace. 

Lithium (Li) ' 

Calcium (Ca) 

Magnesium (Mg) 

Iron ( Fe) 

.Muminum ( Al) 

Sulphate (SO4) 

Chloride rci) 

Carbonate (CO3) 

Metaborate (BO2) 

Silica (Si02) 



Carbon dioxide (CO2) 1, 220 



116 
65 
5. 
19 
74 

549 



13 



1,036.2 



Reacting 
values. 



By 
weight. 



5.4,S 
Trace. 



3.44 

9.54 

2.33 

.58 

.40 

2.09 

18.30 



74 
129 

65 
5.4 

22 

54 
578 



Reacting 
values. 



By 
weight. 



4.65 



.43 



11 



3.69 

10.58 

2.33 

.60 

.46 

1.52 

19.27 



.36 



1-13 

Trace. 

Trace. 

61 

124 

67 

6.7 

8.8 

49 

608 

Trace. 

14 



1,081.6 



815 



Reacting 
values. 



6.22 

Trace. 

Trace. 

3.04 

10.22 

2.40 

.74 

.18 

1.38 

20.28 

Trace. 

.46 



1. Pagoda Spring. Analyst and authority, Winslow Anderson (ISSS). 

2. Pagoda Spring. Analyst, Lanzwurt (1870). Authority, IT. S. Geol. Survey Bull. 32. 

3. Lemon Spring. Analyst and authority, "Winslow Anderson (18S9). 



CONGRESS SPRING (NAPA 14). 

Congress Spring is situated at the base of a low hill of tuff, about 
3 J miles southwest of Napa. It yields about one-half gallon a 
minute of carbonated saline water, and a considerable amount of 
alkaline material forms on the surface near by. The spring has been 
protected by a board curbing, and a small amount of the water has 
been sold locally, but it has been of little importance as a marketed 
water. 

JETNA SPRINGS (NAPA 2). 

Near the head of Pope Valley, about 20 miles in a dii'cct line 
northwest of Jacksons Napa Soda Springs, a large resort has been 
built up at ^Etna Springs (Lidell post office). 

The property, which borders Pope Creek, formerly belonged to 
the ^tna Quicksilver Mining Co., and the locality once produced 
much of the metal. After mining was discontinued in one of the 
tunnels the water in it was observed to be mineralized, and as early 



CAKBO^'AIKD SPRINGS. 157 

as 1878 the locality was resorted to for use of this water. In 
1887 it was put on the market for table use, and since that time 
the propert}' has been extensively improved . There are extensive 
fi^rounds in which are <i;i'ouped several cotta<::os, clubhouse, recep- 
tion hall, and dining hall; and a bathhouse and a swimming plunge 
have been erected beside the creek. The place is within an easy I'ide 
from St. Helena by automobile stage, over a graveled and well- 
graded road. 

The Tunnel Spring is no longer used, but on the southern bank 
of the creek two similar springs, known as the Summerhouse and the 
American Ems, have been surrounded by cemented basins and pro- 
tected by a spring house. The two springs that furnish the water 
for bottling are situated in open land about 700 and 800 yards, 
respectively, northeast of those at the creek, at places that were 
formerly tule grown. The more distant is known as the Potassium 
Spring and is the one whose water is chiefly bottled ; the other is 
called I-ador-a Spring. 

The water of all five of the springs now used is carbonated, tastes 
distinctly mineralized, and is noticeably thermal, but as they are best 
known for their carbonated character they are more properly described 
under this heading. Summerhouse and American Ems springs are the 
warmest, their recorded temperature in 1909 being 92°. Analyses 
of all the springs, including the Tunnel Spring, have been made, 
and are here reproduced in stantlard form. 



158 



SPEIlSrGS OF CALIFORNIA. 



CO o o Oi »o 



OOOOOIM 



-* O O --H O T 



"O o o ^^ oc 00 



^ ooocnio 









o 3 

(2^ 



cooo<^ ooo 

(M CD CO 



CO OO Oi COCO 
CO 'Tt* r-( t^ 



O *^"Z 



n o 



00 (M >-< C^J (M .M O C' '-' 0-. O CO o; 



'cooiccoicocdcocooot-^ 



r-1 -^(M ^ 



O100i-( giO 

<N •* e-i g r-i 



iC to cC ^ 1>- 



'— (NO 
C^J CO 



O 1^ O OS CD 
r-H '^ C-l O (M 



(MO t- (M 



CO C0 05i-t 
(N coco CO 



00 00 









OQ 



Ph.S 



CCoc, 






t; g H t, .g o fe 

jS t- fe 0^ ^-1 ^ cl 



5 fe ^ ^^ 



!>> 






\2.a 



■S O g'i-j 






2^ .^ 



4^4^ .ffi " 



> 






.g.grfl.^1 
sgso ft.g 

n c,A^B Bm 

o o ®— 1 ft-- ■=? 

S « p 3 o o c3 
<K CO E-i H^ Ph i-H 



a 



CARBONATED SPRINGS. 159 

The analyses indicate that the waters arc all of the same gcnei'al 
primary alkaline type, but tlu>y show minor differences in the relative 
proportions of calcium and ma<]i;nesiuni and of sodium and potassium 
and in the content of silica, iron, and aluminum. The Wenzell 
analyses alone report borates, but it is not unlikely that tests for 
borates were not made by the other analysts and that borates are 
reported as carbonates. The great similarity of the three analyses 
by Bauer and the apparent change in composition of the American 
Ems Spring water arc of interest. 

The rocks about ^tna Springs are the altered sediments, opahne 
material, and associated serpentine of the Franciscan formation. A 
short distance northward, near some of the quicksilver workings, 
lava covers the surface. 

WALTERS MINERAL SPRINGS (NAPA 3). 

About 10 miles by road east of ^Etna Springs, on the eastern side 
of the canyon of Pope Creek, there are two small carbonated springs 
that have long been known as Walters Mineral Springs. They 
issue about 150 yards apart and 350 feet above the creek, on the 
side of a ravine in an area of serpentine. The rock has decayed 
sufficiently to form a red clay soil, but many bowlders outcrop on 
the hillsides. The water has a distinctly sweet taste, and the analysis 
tabulated on page 160 shows that it contains a high proportion of 
magnesium, being secondary alkaline in character. 

The magnesian character of the water is worthy of note in con- 
nection with the serpentine at this locality. The association with 
serpentine (a magnesium-bearing rock) of mineral springs having a 
high content of magnesium would be expected, however, and it has 
been already mentioned in the discussion of the relation of the min- 
eral character of snrings to the rocks through which they rise. (See 
p. 160.) 

Walters Mineral Sj)rings have been improved as a resort since 
about 1902. In 1910 there were two new frame buildings, having 
accommodations for 50 people, and a paviUon at the lower spring 
that provided a place for dances and other social gatherings. Water 
from this spring has been bottled and marketed to a small extent for 
table use. 

SAMUEL SODA SPRINGS (NAPA 7). 

About 6 miles southeast of Walters Mineral Springs, and also well 
above Pope Creek but on the other side of its canyon, Samuel Soda 
Springs form another group that has long been known. The place 
has been improved as a resort for a number of years, and the water 
has also been sold as a carbonated table water. 



160 



SPRINGS OF CALIFORNIA. 



Four of the six mineral springs on this property rise close together, 
in cement basins near the bank of a small cascading stream, and a 
fifth spring issues at the opposite edge of the stream. These springs 
range in flow from about 1^ to 6 gallons a minute. The sixth spring, 
which is small and relatively unimportant, issues at the side of a 
ravine 250 yards northward. Small amounts of iron are deposited 
along all the overflow channels. The water of aU the springs is 
carbonated and has a slightly sweet taste that is probably due to 
magnesium. The following analysis of water from one of the four 
main springs shows it to be similar in character to that of one of the 
Walters springs with which it is tabulated, but it is not so strongly 
mineralized. 



Analyses of water from Samuel Soda Sjmngs and Walters Mineral Springs, Napa 

County, Cal. 

[Constituents are in parts per million.] 



Temperature 

Propertie? of reaction: 

Primary salinity 

Secondary salinity. . . 

Tertiary salinity 

Primary alkalinity. . . 
Secondary alkalinity. 
Tertiary alkalinity . . . 



Constituents. 



Sodium (Na) 

Potassium (K) 

Lithium (Li) 

Barium (Ba) 

Strontium (Sr) 

Calcium (Ca) 

Magnesium (Mg).. 

Iron(Fe) 

Manganese (Mn). . 

Sulphate (SO4) 

Chloride (CI) 

Carbonate (CO3).. 
Metaborate (BO3). 
Phosphate (POj).. 
Silica (SiOs) 



27 


12 
61 
425 



14°C. (58°F.) 

22 


15 
63 
400 



weight. 



219 

23 

Trace. 



Trace. 
14 
186 
7.9 



31 

222 
578 
Trace. 
6.1 

82 



1,369 



Carbon dio.xide (CO.) 2, 370 



Reacting 
values. 



By 
weight. 



9.52 

.59 

Trace. 



Trace. 

.70 

15.29 

.28 



288 
2.5 
Trace. 
.7 
Trace. 
50 
232 
5.5 
.1 



.65 

0.26 

19.28 

Trace. 

.19 

2.72 



262 

807 

Trace. 

2.7 

114 



1,764.5 



107. 80 



2,920 



Reactiue 
values. 



12.52 

.06 

Trace. 

.01 

Trace. 

2.49 

19.08 

.20 

Trace. 



7.39 

26. 88 

Trace. 

.09 

3.78 



1. Samuel Soda Springs; probably principal spring. Analyst, E. W. Hilgard. Authority, 12th Cal. 

2. Walters Mineral Springs: probably lower sp ing. Analyst, G. E. Colby. Authority, advertising 
matter. 



The high content of magnesium is to be expected, for the springs 
issue from serpentine in an area of altered sediments that form the 
principal rocks of this region. There are quicksilver prospects in a 
deep ravine a quarter of a mile to the southeast, but the deposition of 
the cinnabar probably has no close association with the existence of 
the mineral springs. 



CAKBONATED SPEINGS. 



161 



NAPA ROCK SODA SPRINGS (NAPA 9). 

Napa Rock Soda Springs, known also as Priest Soda Springs, issue 
on the hillsitle that borders a small valley about 6 miles in a direct line 
south of Sanuiol Soda Springs. A spring that has a temperature of 
79° and a discharge of about 15 gallons a minute here rises in a rock- 
walled basin 7 feet in diameter. Much gas rises with the -water, which 
is moderately carbonated and also tastes distinctly of magnesium. 
The overflow channel is lined with iron-stained cemented gravel. In 
1910 a smaller spring 40 yards southward was covered with boards, 
and a pipe line extended from it down the slope to a small bottling 
house. The following analysis shows that the water is secondary 
alkaline in character, magnesium being present in relatively large 
proportion. 

Analysis of water from main spring, Napa Rock Soda Springs, Napa County, Cal. 
[Analyst, W. B. Rising. Authority, advertising matter. Constituents are in parts per million.] 



Properties of reaction: 

Primary salinity 

Secondary salinity 

Tertiary salinity 

Primary alkaliuity 

Secondary alkalinity 

Tertiary alkalinity 

Constituents. 

Sodium (Na) 

Calcium (Ca) 

Magnesium (Mg) 

Aluminum ( Al) 

Sulphate (SO4) 

Chloride (CI) 

Carbonate (CO3) 

Carbon dioxide (CO2) : 

a Reported 95; probably a typographical error 



(?) 



By 

weight. 



Reacting 
values. 



736 

401 
1,069 

39.5 

633 

398 
3,464 



32.00 
19.98 
87.87 
1.06 
13.18 
11.22 
115. 45 



6, 710. 5 



Present. 



PHILLIPS SODA SPRINGS (NAPA 8). 

About 350 yards north of Napa Rock Soda Springs and 100 feet 
higher up the slope are two carbonated springs that are known as 
Phillips Soda Springs, The principal spring rises in an oval, stone- 
walled basin about 4 by 10 feet across; the other forms a pool in the 
soil, 25 yards away. In 1910 an old bathhouse, a residence, and two 
other buildings stood near the springs, but the property had evidently 
been deserted for a number of years. The waters are carbonated and 
are apparently similar in character to those of the Napa Rock Springs, 
but they have formed a large deposit in which the cementing material 
is a carbonate of magnesia instead of the much more common car- 
bonate of lime. 



35657°— wsp 338—15- 



-11 



162 SPEINGS OP CALIFOElSriA. 

The following analysis of the material by Roger C. Wells indi- 
cates that at least a part of the deposit has come into a stable con- 
dition with regard to its content of moisture and may be the mineral 
hydrogiobertite (MgC03.Mg(OH)2 + 2H20), though other parts of the 
specimen examined had a somewhat different composition.^ A speci- 
men that was examined microscopically by W. T. Schaller appeared 
to consist of two intergrown minerals. 

Analysis of material from spring deposit at Phillips Soda Springs, Napa County, Col. 
[Analyst, R. C. Wells, 1910.] 

Insoluble in hydrochloric acid ^ 25. 37 

Soluble in hydrochloric acid : 

Iron and alumina (FeaOg+ALOg) 1. 88 

Calcium oxide (CaO) 2. 57 

Magnesium oxide (MgO) 31. 81 

Carbon dioxide (CO,) ' 18. 07 

Sulphate (SOJ None. 

Water (HoO) 19. 94 

99. 64 

Along the front of this deposit, where it has been cut into by the 
surface water, there is a bluff that exposes a structure resembling 
a stockwork, in which veins and masses of the cementing material 
inclose fragments of dark shale. 

Phillips and Napa Rock springs issue at the lower border of an 
area of serpentine that apparently overhes the shale forming the 
lower portion of the hills. The association of serpentine with mag- 
nesium waters is here again clearly shown, but the large spring 
deposit of a magnesium carbonate is believed to be an uncommon 
formation. The only other notable one of the kind that was observed 
in the State was near the Hot Springs at Elgin mine, in Colusa 
County, but the deposit at Phillips Springs differs from the hard 
compact material found there. 

GAILLAITMES SODA SPRINGS (NAPA 6). 

In a ravine about 6 miles northwestward across the hills from 
Phillips springs on the GaiUaume ranch are two or three small car- 
bonated and sulphureted springs that have been occasionally visited 
by campers, but in 1910 they had not attained importance. The 
rocks at these springs are part of the sedimentary series that covers 
miost of this region. 

TOLENAS SPRINGS (SOLANO 1). 

In the Coast Ranges there are two notable deposits of calcium 
carbonate in the form of onyx marble or Mexican onyx which seem 
to be essentially spring deposits and near which carbonated water 

1 Wells, R. C, A new occurrence of hydrogiobertite: Am. Jour. Sci., 4th ser., vol. 30, pp. 189-190,1910. 

2 The insoluble portion had the appearance of soft grains resembling shale. 



CARBONATED SPRINGS. 



163 



still issues. One of those is at Tolenas Springs, in Solant) County, 
about 6 miles north of Fairfield. The material outcrops over an area 
about 100 yards in diameter, on slopes near the top of a range of 
hills composed of soft shale and sandstone, and carbonated saline 
water seeps from two shallow pools at the deposit. The principal 
spring, however, is on the hillside 300 yards westward and 50 feet 
higher, where a pit has been excavated a few feet deep in a small 
deposit of the onyx marble. In 1909 separate pipes conducted the 
water and the carbon dioxide to a bottling house a short distance 
away. Only sedimentary rocks were observed near these springs, 
but "a breccia of shale, sandstone and volcanic ash, cemented 
by lime and traversed by veins and bunches of aragonite (?)" has 
been mentioned by Day.^ Considerable stone has been shipped 
from the deposit, but the material is too cavernous to be suitable 
for extensive use as a decorative stone, and quarrying was discontinued 
a number of years ago. Most of the stone is light colored and trans- 
lucent, with white, cloudy mottling, but some darker material was 
noticed. Banded aragonite, several inches thick, has been deposited 
in some places on more compact calcite. The analysis of the material 
tabulated on page 165 with that of similar material from San Luis 
Obispo County represents a specimen of the calcite. 

Another carbonated saline spring emerges in a ravine 300 yards 
southeast of the quarry and has been used as a watering place by 
range cattle aiid horses. It has built up a deposit of lime carbonate 
several vards in diameter. 



Analyses of ivater from Tolenas Springs, Solano County, Cal. 
fConstituents are in parts per million.] 



Temperature 

Properties of reaction: 
Primary salinity . .. . . 
Secondary salinity . . . 

Tertiary "salinity 

Primary alkalinity. . . 
Secondary alkalinity. 
Tertiary "alkalinity . . 



17° C. (62° F.) 

59 



19 

22 
13 



Constituents. 



Sodium (Na) 

Potassium (K) 

Calcium (Ca) 

Magnesium (Mg).. 

Iron (Fe) 

Aluminum (Al)... 

Chloride (CI) 

Iodide (I) 

Carbonate (CO,).. 
Metaborate (BO2). 
Silica (Si02) 



Carbon dioxide (CO2). 



By 
weight. 



1,760 

65 

342 

57 

7.3 

10 

2,068 

23 

1,154 

139 

33 



5,658.3 



266 



Reacting 
values. 



By 
weight. 



76.55 
1.67 

17.03 

4.70 

.26 

1.11 

58.34 
.18 

38.45 
3.24 
1.09 



1,930 

59 

331 

54 

5.3 

8.7 

2,288 

27 

1,151 

150 

27 



6,031.0 



12.09 



287 



Reacting 
values. 



83.92 

1.51 

1G.52 

4.42 

.19 

.96 

64.51 

.21 

38. 36 

3.48 

.91 



1. Main Spring. Analyst and .authority, Winslow Anderson (1888). 

2. Main Spring. Analyst, J. Hewston, jr. (prior to 1888). Authority, U. S. Geol. Survey Bull. 32. 



1 Day, W. C, Stone: U. S. Geol. Survey Twentieth Ann. Rept., pt. 6 (continued), p. 288, 1899. 



164 SPRIISrGS OF CALIFORlSriA. 

KESSLEB SPRINGS (SAN LUIS OBISPO 10). 

The other group of sprmgs at which onyx marble has been formed 
is at Kessler Springs — better known as the Kessler Mexican onyx 
quarries — in San Luis Obispo County, about 20 miles "northeast of 
Arroyo Grande, among hills of sandstone and shale that are probably 
of Tertiary age. The principal outcrop of the onyx marble forms a 
ledge, several yards in height and extent, at the side of a small ravine ; 
a smaller exposure of veins of the material, several inches in tliick- 
ness, appears in a dark mud shale in a prospect trench a quarter of 
a mile northward. Between these two places are several outcrops 
of the stone, at three or four of which issue small amounts of 
slightly carbonated sahne water. During the dry season the run-off 
channels are crusted with deposits that consist largely of common 
salt. 

The property was filed on as a mineral claim in the early seventies, 
and, a number of slabs of the stone were taken out by means of steel 
blades and emery, but the material contains too many cavities to 
enable it to compete as a merchantable stone with that from other 
quarries, and development ceased about 1895. The material at the 
prospect trench is almost pure wliite, but at the larger exposure, 
where most of it was obtained, it is more translucent, and has a 
mottled, cloudy appearance that is due to the inclusion of a small 
amount of clay. 

Although the amount of water that now issues is very small, the 
fact that the onyx marble is essentially a spring deposit entitles the 
locality to description in this paper. 

Two minor onyx marble deposits, probably formed by mineral 
springs, have been worked. One of these is near the western side of 
Sacramento River, near Shasta Springs, and was known as the Griffin 
quarry. Material large enough only for paper weights and similar 
small articles was obtained at this quarry. The other locahty is near 
the Elgin quicksilver mine, about 30 miles west of Wilhams in Colusa 
County.^ 

The two analyses of Cahfornian onyx marbles that are available 
are presented in the following table : 

1 In the description of the deposits at the hot springs near Bridgeport, Mono County (p. 134), Merrill has 
heen quoted concerning the formation of onyx marble. He states that most of the onyx marbles are of 
caleite, not aragonite. Microscopic examination of material from the Bridgeport, Tolenas, and Kessler 
quarries, and determinations of the specific gravity of specimens show that nearly all of it is caleite, but 
a small specimen from the Tolenas quarry consists of two nearly equal bands of aragonite and caleite. 



CARBONATED SPRINGS. 



165 



Analyses of onyx marbles from Kessler Springs and Tolenas Springs, CalM 
[R. L. Packard, analyst.] 



Kessler 
Springs. 



Tolenas 
Springs. 



Color 

Structure . 



Hardness 

Specific gravity 

Analysis as reported: 

Calcium curbonate (CaCOs) 

Magnesium carbonate (MgCOs) 

Iron carbonate ( FeCOs) 

Manganese carbonate (MnCOa) . 
Strontium carbonate (SrCOa)... 

Barium carbonate (BaCOs) 

Calcium phosphate (CasCPOi);). 
Water (H2O) 



White. 
Microcolum- 
nar. 
3.50 
2.72 

93.68 

1.43 

3.93 

.06 



Dark amber. 

Granular and 
columnar. 
3.25 
2.70 

95.48 
2.20 



.25 



Kecalculated form: 
Iron(Fe) 

Manganese (Mn) . 

Calcium (Ca) 

Magjnesiiun (Mg). 

Barium (Ba) 

Strontium (Sr)... 
Carbonate (CO3) . 
Phosphate (POi). 
Water (H2O) 



1.897 

.029 

37. 612 

.412 



59. 290 
.110 



99.350 



1.59 
0.11 



0.37 



99.75 



38. 192 
.634 
.077 
.943 

59. 534 



.370 



99.750 



o Merrill, G. P., The onyx marbles: Their origin, composition, and uses, both ancient and modem: 
U. S. Nat. Mas. Rept. for 1893, table facing p. 559. 



LYTTON SPRINGS (SONOMA 9). 

Lytton Springs are one-half mile west of Lytton station, in the 
hills that border the valley of Russian River, in Sonoma County. 
A number of years ago there was a resort at the springs, and the 
place was known as Geyser Spa. In 1910, however, the property 
was conducted as the Golden Gate Orphanage, under the auspices 
of the Salvation Army. The principal spring rises in the bed of a 
small stream at the northern side of the grounds. The water was 
formerly bottled in a house directly over the spring, and in 1910 it 
was still marketed, but the bottHng house was not in repair and the 
water was piped a few yards below to a small shelter, where it formed 
a drinking fountain. The w^ater tastes moderately carbonated and 
distinctly sahne. Analysis 1 in the following table probably repre- 
sents water from this spring and indicates that it is primary alkahne 
saUne in character. Two other smaller carbonated springs that rise 
on the hillside half a mile north w^est ward have been unused for 
several years and when \"isited w^ere of Uttle importance. Analysis 2 
in the table, wliich probably represents water from one of these 
springs, indicates that it is much less strongly mineralized than the 
main spring and that primary saUnity, primary alkaUnity, and 
secondary alkalinity are about equally prominent as properties. 



166 



SPRINGS OF CALIFOENIA. 



Analyses of water from Lytton Springs, Sonoma County, Cal. 
[Constituents are in parts per million.] 



Temperature 

Properties of , reaction : 

Primary salinity 

Secondary salinity. . . 

Tertiary salinity 

Primary alkalinity . . 
Secondary alkalinity , 
Tertiary alkalinity . . 



Constituents. 



17° C. (62° F.) 

45 


39 
16 
■ 507 



By 

weight. 



Reacting 
values. 



27 





42 

31 

High. 



By 
weight. 



Reacting 
values. 



(?) 



By 
weight. 



Reacting 
values. 



Sodium (Na) 

Potassium (K) 

Lithium (Li) 

Ammonium (NH4). 

Calcium (Ca) 

Magnesium (Mg). . . 

Iron(re) 

Aluminum (Al) 

Sulphate (SO4) 

Chloride (CI) 

Carbonate (CO3) . . . 
Metaborate (B02)«- 
Silica(Si02) 



Carbon dioxide (CO2) 6, 430 



1,104 

35 

Trace. 

6.0 

85 

63 

18 

62 

153 

822 

975 

32 

138 



47.98 

.89 

Trace. 

.33 

4.24 

5.17 

.63 

6.87 

3.19 

23.21 

32.51 

.75 

4.58 



210 
Trace. 



9.13 
Trace. 



1.70 

2.47 
.60 



1.55 
2.30 
1.11 



93 
310 



2.62 
10.32 



39 
103 
293 



.81 
2.90 
9.77 



1.03 



3,493 



804 



752 



292. 50 



Excess Present. Present 



a Reported as borates. Recalculated from Na2B407. 

1. Main spring. Analyst and authority, Winslow Anderson (1888). 

2. Minor spring. Analyst and authority, Winslow Anderson (1888). 

3. Minor spring. Analysts, Bauer and Price, date not given. Authority, Winslow Anderson. 

Shale, overlain by quartzitic and cherty gravel, is exposed along 
the creek near the main spring, and sedimentary rocks apparently 
form the hills near by. 

CARBONATED SPRING NEAR LITTLE SULPHUR CREEK (SONOMA 7). 

A small carbonated spring issues at the side of a gully near Little 
Sulphur Creek, on the Nelson & Olsen ranch, 3 miles east of Geyser- 
ville. It has been used only as a local drinking spring, has not been 
improved, and is not specially noteworthy. 

ALDER GLEN SPRINGS (SONOMA 2). 

Alder Glen Springs form a resort in a small canyon 3 miles, north- 
west of Cloverdale. In 1909 a two-story frame hotel, annex, and 
several cottages and tents furnished accommodations for about 75 
guests, and a pavilion and hall were also provided. On the southern 
side of the stream channel the face of the bank has been cemented 
around four basins a yard apart that discharge into a common over- 
flow channel. The springs differ somewhat in taste, but all are car- 
bonated and are also faintly sulphureted. Small amounts of iron are 
deposited in the basins and along the overflow channel. 



CARBONATED SPRINGS. 167 

Besides its use on the orounds for drinking (ho w^ater has been 
bottled and sold locally. 

The rocks exposed along the canyon are cruslied and altered sand- 
stones and shales, with a little cherty material, the springs issuing 
from sandstone. 

DFNCAN SPRINGS (MENDOCINO 31). 

Duncan Springs are situated 2 miles west of south from Hopland, 
on slopes that overlook Russian River valley. The property has been 
run as a resort since the eighties. Several additional buildings have 
been erected during recent years, so that in 1909 a hotel, annex, and 
several cottages provided rooms for about 100 guests. 

There are two principal springs, which are known as Magnesia 
Spring and Soda Spring, and two minor slightly used springs. The 
Magnesia Spring issues at the eastern end of a pavilion 175 yards 
south of the hotel. Two cemented basins have been constructed in this 
place on a sloping surface of serpentine. Their combined yield is 
perhaps one-haK gallon per minute of water that is moderately 
carbonated and magnesic in taste. This water has for a number of 
years been shipped to San Francisco and carbonated and bottled for 
table use. The analysis (p. 168) shows that it is essentially a magnesic 
alkaline water. The unusually small content of sodium reported is a 
remarkable feature of the analysis. 

The Soda Spring is higher up the slope, in a ravme 500 yards to the 
southwest. like the Magnesia Spring, it also issues from serpentine 
and is protected by a rock-walled basin. Its water is strongly car- 
bonated and tastes distinctly of iron, and considerable iron is also 
deposited in the spring and along its overflow channel. This constit- 
uent renders the water unsuitable for botthng and sale, as it stains 
the bottles, but the water is used on the grounds for drinking and is 
also piped to a bathhouse near the hotel and heated for bathing. 

The following analyses of the water show noteworthy differences 
in the character of the two springs, the Soda Spring possessing both 
primary and secondary alkalinity, whereas the Magnesia Spring has 
no reported primary alkahnity but high secondary and tertiary 
alkalinity. 



168 



SPRINGS OF CALIFORNIA. 



Analyses of water from Duncan Springs, Mendocino County, Col. 
[Constituents are in parts per million.] 



Temperature 

Properties of reaction: 

Primary salinity 

Secondary salinity . . . 

Tertiary salinity 

Primary alkalinity . . . 
Secondary alkalinity . 
Tertiary alkalinity . . 



Constituents. 



Sodium (Na) 

Calcium (Ca) 

Magnesium (Mg) . 

Iron(Fe) 

Sulphate (QOi) . . 

Chloride (CI) 

Carbonate (CO3). 
Silica (SiOs) 



Carbon dioxide (CO2) - 



(?) 



By 

weight. 



366 

482 

223 

Trace. 



178 

1,597 

Trace. 



Reacting 
values. 



15.90 

24.04 

18.33 

Trace. 



5.03 

53.24 

Trace. 



Present. Present 



14° C. (57° F.) 

9 



18 
73 
12 



By 

weight. 



363 

496 

220 

Trace. 



178 

1,610 

Trace. 



2,867 



153 



Reacting 
values. 



15.80 

24.77 

18.11 

Trace. 



5.02 

63.66 

Trace. 



By 
weight. 



11 

67 

268 



22 

18 

746 

119 



1,251 



311 



Reacting 
values. 



0.48 
3.34 
22.02 



.46 
.51 

24.87 
3.95 



1. Soda Spring. Analyst, J. A. Bauer (?). Authority, Bull.U. S. Geol. Survey No. 32. 

2. Soda Spring. Analyst and authority, Winslow Anderson (1889). 

3. Magnesia Sprmg. Analyst, A. W. Thatcher (?). Authority, 10th Cal. 

There is a small sulphur spring a short distance above the Soda 
Spring, and a more alkahne spring farther down the ravine, but these 
two have been unimproved and seldom visited. 

The country rock of the hillside on which this resort is situated 
seems to be mainly serpentine, but between the paviUon and the 
hotel there is a band of hornblende schist 20 yards wide, and a small 
amount of siUceous sandstone float was noted on the slopes near hy. 

Mcdowell springs (mendocino 32). 

McDowell Springs are situated at the southern edge of McDowell 
Valley, about 5 miles southeast of Hopland. Tliree principal springs 
issue at the northern edge of the main creek through the valley, at 
the base of a 30-foot bank. In 1909 one of the springs was improved 
by a brick curbing, which formed a pool about 4 feet in diameter and 
2 feet deep. Much gas rises in large bubbles in the pool and is prob- 
ably carbon dioxide, for it quickly extinguishes a flame and the 
water is strongly carbonated. The iron content has stained the 
surface of the ground near by and the water is said to precipitate too 
much iron to make it suitable for botthng. The following analysis 
shows the water to be of the secondary alkaline type, only moder- 
ately mineralized. The relative prominence of iron and sihca makes 
the water of chemical interest. 



CARBONATED SPRINGS. 



169 



Analysis of water from main spring at McDowell Springs, Mendocino County, Cat. 

[Analysts, Curtis and Tompkins, 1908. Authority, advertising matter. Constituents are in parts per 

million.] 



Properties of reaction: 

I'rimary salinity 

Secoiuiiiry salinity 

• Tertiary siiliiiity 

Primary alkalinity 

SecoiKhirv alkalinity 

Tertiary alkalinity 

Constituents. 

Sodium (Na) 

Potassium (K) 

Lithium (Li) 

Ammonium (NH4) 

Barium (I3a) and strontium (Sr) 

Calcium (Ca) 

Magnesium (Mg) 

Iron ( Fe) 

Aluminum ( Al) 

Manganese (Mn) 

Sulphate (SOi) 

Nitrate (NO,) and nitrite (NO2) 

Chloride (CI) 

Carbonate (CO3) 

Metal orate (BO2) 

Phosphate ( POi) 

Silica (Si02) 

Carbon dioxide (CO2) 

Hydrogen sulphide (HjS) 



5 


3 

92 
394 



By 

weight. 



Reacting 
values. 



7.7 
2.9 
Trace. 
Trace. 
Traces. 
40 
31 
53 
2.8 
.1 
5.3 
0.0 
5.5 
206 
Trace. 
.7 
69 



.34 

.07 

Trace. 

Trace. 

Traces. 

2.01 

2.59 

1.90 

.31 

Trace. 

.11 

.00 

.16 

6.86 

Trace. 

.02 

2.28 



424 



336 




15.30 



Thirty yards below the main spring a similar spring has formed a 
small natural basin, and at about the same distance upstream car- 
bonated water seeps from the bank and has heavily iron stained it. 
Other seepages that issue along the creek bed have stained it with 
iron for a cUstance of nearly a quarter of a mile above the main spring. 

Soft shale that is overlain by gravel is exposed along the creek. 
At a few places several hundred yards eastward, upstream from the 
springs, inflammable gas is said to rise, making its presence known 
by bubbles when the ground is wet. 

The property has been open as a resort since 1902 or 1903. In 
1909 tent houses and a dining room provided accommodations for 
about 50 people. 

CARBONATED SPRINGS NEAR FELIZ CREEK (MENDOCINO 28). 

About 3 miles west of Hopland, in a ravine on the slopes above 
Feliz Creek, are two small springs. One of these springs is notice- 
ably carbonated and deposits a little iron along its channel, whereas the 
other is less distinctly carbonated but tastes noticeably of hydrogen 
sulphide. The two springs are about 20 yards apart, on opposite sides 
of the ravine, and issue from banks of crushed sandstone and siliceous 
shale, near the side of a wagon road. In 1909 the carbonated spring 
formed a box-curbed drinking pool. A brick-lined basin 3 by 6 feet 
had been constructed at the sulphureted spring, and a pipe led from 
it to the roadside. 



170 



SPRINGS OF CALIFORNIA. 



CARBONATED SPRINGS ON RUSSIAN RIVER (MENDOCINO 29). 

Carbonated water issues from gravel at the western edge of Russian 
Eiver, 2| miles north of Hopland, in springs locally known as Human- 
ity Springs. In 1907 an excavation was made at the place so that 
the water was accessible, and it was considered to be of medicinal 
value. During the summer of 1910 the springs were again rendered 
accessible, and some of the water was bottled. 

The following analyses represent water from two springs at this 
locality that issued a few yards apart in 1907: 

Analyses of toater from carbonated springs on Russian River, Mendocino County, Cal. 

{Analyst, G. E Colby (1907). Authority, owner of springs. Constituents are in parts per million by 

weight.] 



Properties of reaction: 

Primary salinity 

Secondary salinity 

Tertiary salinity 

Primary alkalinity 

Secondary alkalinity 

Tertiary alkalinity 

Potassium sulphate (very small), sodium sulphate, etc 

Sodium chloride 

Sodium carbonate 

Calcium and magnesium carbonates (chiefly) and calcium sul- 
phate (small) 

Silica 

Organic matter and combined water 

Carbon dioxide 



Large. 
(?) 



(?) 

Dominant. 
Large. 



Probably dominant. 
(?) 


(?) 

Large. 
Large. 



34 
Trace. 
5.8 

77 
45 
24 


100 
2.9 
2.9 

70 
38 
20 


185.8 


233.8 



Excess. 



Excess. 



1 and 2. Analyses of separate springs. 

ORNBAUNS MINERAL SPRING (MENDOCINO 36). 

Ornbaxms Mineral Spring is located at the lower end of a small 
meadow valley, 20 miles northwest of Cloverdale. The sprmg issues 
near the southern side of the creek that runs through the meadow 
from soft, shaly sandstone that has been exposed by removing the 
thin layer of alluvium in order to obtain a rock drinking basin. The 
water is moderately carbonated and has noticeably iron stained the 
near-by surface. 

In the summer of 1909 a hotel of about 20 rooms was built on the 
edge of the valley. 

CARBONATED SPRINGS ON GARCIA RIVER (MENDOCINO 34). 

About 3i miles southwestward, downstream from Ornbauns spring, 
carbonated water seeps from the banks above Garcia River. One 
spring of appreciable flow also issues near the water's edge but is 
submerged during stormy periods. The springs are accessible by a 
trail but are seldom visited. A smaU alkaline deposit from the water 
makes the place a local deer lick. The rock from which the springs 



CARBONATED SPRINGS. 171 

issue consists of the crushed sediments that cover a large part of th(^ 
region. 

CARBONATED SPRING NEAR BOONVILLE (MENDOCINO 26). 

A small carbonated spring rises on the Hotel ranch, near Boonville, 
about 25 miles northwest of Cloverdale. It has not been improved, 
however, and has been used only occasionally for drinking. 

SINGLEYS SODA SPRING (MENDOCINO 27). 

Smgle^^s Soda Sprmg is on the main road between Ukiah and 
BoonAolle, about 5 miles northeast of the latter place. There has 
been a roadhouse near the spring for a number of years and the place 
is well known to travelers through this region. The spring has been 
improved only for drinking. 

VICHY SPRINGS (MENDOCINO 24). 

Vichy Springs form a resort that has been established for many 
years on Sulphur Creek, 3 miles northeast of Ukiah. In 1909 a small 
hotel and several cottages provided accommodations for 50 guests, 
and tub baths were suppUed by the two prmcipal springs, which 
rise on the southern side of the creek, about 200 yards southeast of the 
hotel. One of them, known as Ardeche Spring, rises in a cemented 
basin about 5 by 15 feet in size and 2 feet deep and supplies half a 
dozen tubs in a bathliouse beside it. Many bubbles rise with the 
water, which is shghtly clouded as if by a small precipitate of iron, 
and a slight deposit, probably of calcium carbonate, forms on its 
surface. The water is noticeably carbonated and slightly alkaline in 
taste. Its discharge is about 8 gallons a minute, and the temperature 
is 90°. 

About 45 yards southeastward, upstream from Ardeche Spring, 
Yichy Spring rises m a pool of irregular shape, about 6 by 10 feet 
in size, in a natural grotto of Imie carbonate. It is said to have 
formerly issued at a point 3 or 4 yards farther west but changed to 
its present outlet at the time of a small earthquake. The earthquake 
of April 18, 1906, is said not to have affected it, however. When 
visited, the water of Vichy Spring was somewhat clearer than that of 
Ardeche Spring, but a more noticeable deposit of iron was formed. 
Its recorded temperature was 88°, being slightly lower than that of 
Ardeche Spring, but its discharge was approxmiately tmce as great. 
Because of the temperature of the waters of these main sprmgs they 
are sho%vn on the map (PI. Ill, in pocket) as thermal-carbonated, 
but they are best knoAvn for their carbonated character. 

The water of Vichy Spring is kept flowing through tubs m a bath- 
house beside it, when they are in use. A tingling sensation that is 
caused by small bubbles of carbon dioxide which collect on the bather 



172 



SPRINGS OF CALIFORNIA. 



is locally ascribed to an electric property of the water. Two other 
carbonated springs rise in the gravel at the creek edge opposite Vichy 
Spring, but they have not been improved. They yield flows of about 
one-half gaUon and 8 gallons a minute and have the same tempera- 
ture as Vichy Sprmg. There is also a small seeping pool known as 
the Arsenic Spring on the bank 20 yards westward from Ardeche 
Spring, but it has been only slightly used. A quarter of a mile south 
of east from the mam group, on the hillside 25 or 30 feet above the 
creek, a third spring of importance issues in a rock-walled basin that 
is protected by a roof, and yields perhaps a quarter of a gallon a min- 
ute. Like the other springs, it deposits iron and its water has a 
slightly alkaline taste. It is known as Crystal Spring and is a favor- 
ite for drinking, for its water is cool (59°) and pleasantly carbonated. 
Another small pool is formed by a seepage spring on the hillside 30 
yards above Crystal Spring, but it has not been improved. 

The following analyses of the three principal springs show their 
waters to be primary alkaline in character: 

Analyses of water from Vichy Springs, Mendocino County, Cal. 
[Constituents are in parts per million.] 



Temperature 

Properties of reaction: 

Primary salinity 

Secondary salinity. . 

Tertiary salinity 

Primary alkalinity. . 
Secondary alkalinity 
Tertiary alkalinity. . 



Constituents. 



Sodium (Na) 

Potassium (K) 

Calcium (Ca) 

Magnesium (Mg). . 

Iron(Fe) 

Aluminum (Al)... 
Sulphate (SO4).... 

Chloride (01) 

Carbonate (CO3).. 
Metaborate (BO2). 
Silica (Si02) 



32° C. (90° F.) 





73 
18 
115 



34° C. (93° F.) 

10 



73 
17 
107 



32° C. (90° F.) 



15° C. (59° F.) 



Carbon dioxide (CO2) 2,128 96.70 1,962 



(?) 



(?) 



By 
weight. 



1,654 

Trace. 

122 

112 

Trace. 

Trace 

Trace. 

285 

2,375 



117 



4,665 



React- 
ing 
values. 



By 
weight. 



71.90 

Trace. 

6.11 

9.19 

Trace. 

Trace. 

Trace. 

8.05 

79.15 



3.88 



1,649 
.8 
124 
97 
.6 
Trace. 
4.2 
298 
2,321 
Trace. 
101 



4, 595. 6 



React- 
ing 
values. 



By 
weight. 



71. 64 

.02 

6.20 

- 7.98 

.02 

Trace. 

.09 

8.41 

77.36 

Trace. 

3.35 



1,141 
20 
133 

48 



204 

1,612 

66 

54 



3,287.1 



React- 
ing 
values. 



By 
weight. 



49.60 

.51 

6.64 

3.95 

.33 



1,248 

19 

149 

58 

7.9 



5.75 

53.74 

1.54 

1.79 



250 
1,756 



.3,587.9 



React- 
ing 
values. 



54.26 

.48 

7.42 

4.74 

.28 



7.07 

58.54 

1.57 

1.06 



1. Vichy Spring. Analyst, John Hewston. Authority, U. S. Geol. Survey BuU. 32. 

2. Vichy Sprini;. Analyst and authority, Winslow Anderson (1889). 

3. Ardeche Spring. Analyst, Price & Son. Authority, advertising matter. 

4. Crystal Spring. Analyst, Price & Son. Authority, 12th Cal. 

Water from these springs has not been bottled commercially, chiefly 
perhaps because the iron and calcium it contains stain the bottles 
and injure its sale. 



CARBONATED SPRINGS. 173 

The rocks of the locaUty are soft sandstones and clay shales. 
Along the creek for some distance below the springs there is a con- 
glomerate that has probably been cemented by lime carbonate de- 
posited from the spring watei-. 

GOBBIS SODA SPRING (MENDOCINO 23). 

A small carbonated sprmg, known as Gobbis Soda Spring, rises at 
the base of the hills a mile southwest of the business portion of 
Ukiah. A brick-lined, tunnel-like basin has been constructed in the 
bank, and in summer the spring is visited for drinking water. As is 
true at most of the other carbonated springs, there is considerable 
iron stam along its outflow channel, but the water does not seem to 
be strongly minerahzed. The rock at the locality is soft, light- 
colored shale that yields a clay soil. 

CARBONATED SPRINGS AT SHOEMAKER DELL (MENDOCINO 22). 

At Shoemaker Dell, a mountain resort in the hills 6 miles north- 
west of Ukiah, there are a number of carbonated springs that are used 
for drinkmg. They are cool and of small flow, like most of the springs 
of the locahty. One or two of the springs are said to be magnesic, 
and magnesium, derived from serpentinous material associated with 
the sedimentary series, may be present in unusual amount. Accom- 
modations for about 50 guests were provided at the property in 1910. 

CARBONATED SPRINGS AT HAZEL HILL (MENDOCINO 25). 

Three small springs that are used for drinking are situated at Hazel 
Hill, a small mountain resort about 35 miles northwest of Cloverdale. 
Only one spring has been improved by a cement basin, but they all 
furnish cool drinking water. The principal spring is moderately car- 
bonated; the other two are respectively sulphureted and ferruginous 
in character. 

CARBONATED SPRINGS NEAR WENDLIN6 (MENDOCINO 21). 

Near Wendhng, a lumbering settlement about 45 miles northwest 
of Cloverdale, there are two or three small carbonated springs. One 
of these was formerly visited by picnic parties, but in recent years it 
has become neglected and partly filled up. A 200-foot well that 
furnishes part of the water that suppUes a mill pond in the neighbor- 
hood also yields water that is carbonated. 

BAKER MINERAL SPRINGS (MENDOCINO 17). 

Baker Mineral Springs are about 18 miles by road east of WilUts, 
on the banks of a stream that is tributary to Tomki River. The 
place has been a small camping resort for several years, and there are 
five small mineral springs on the property. At the lowermost spring 



174 SPEHSTGS OF CALIFOENIA. 

a collecting tank and a bathhouse containing two compartments 
have furnished means for bathing. The water issues from dark shale 
that is here exposed beside the creek and deposits considerable hme 
carbonate. The two principal drinking springs are at the camp 
grounds, which are a quarter of a mile southward up the ravine, and 
issue from seams in coarse-textured sandstone, one of them at the 
creek edge, the other about 25 yards farther upstream and 3 or 4 
yards from the creek. Both are carbonated and deposit considerable 
iron. On the slopes within 100 yards of these springs there is a smaR 
area of mica schist and pyroxene rock associated with outcrops of 
cherty material, which is worthy of note in connection with the 
deposits of iron in the basins of the springs. A seeping carbonated 
spring issues in a branch gully about 150 yards above the principal 
drinking springs, and 50 yards farther up the main ravine the fifth 
spring issues from a bank of sandstone. Like the two principal 
springs, this spring deposits considerable iron, and, like the lowest 
one, it deposits also small amounts of hme carbonate. The water of 
aU of the springs is cool, and the flows are only a quarter of a gaUort 
to 2 gallons a minute. 

SALMON CREEK MINERAL SPRINGS (MENDOCINO 18). 

A small camping resort has been built up at Salmon Creek Mineral 
Springs about 12 miles east of WiUits. Two small mineraUzed 
springs on the property are known, respectively, as Black Sulphur 
and Soda and Iron, and are used during the camping season as drink- 
ing springs. They are similar in mode of occurrence to Baker Mineral 
Springs, a few miles northward, but the sulphureted nature of one of 
the springs makes it similar in general character to springs farther 
west on a branch of Deep Creek, which are described with the sulphur 
springs (p. 258). 

CARBONATED SPRINGS AT TRAVELERS HOME (MENDOCINO 13). 

At Travelers Home (Hearst post office), which is a small mountaiiL 
resort 14 miles by road northeast of Wilhts, there are about a dozen 
small carbonated springs. Several of them are used for drinking, but 
they have not been otherwise developed. The locaUty, hke that of 
the other carbonated springs in the mountains eastward from WilUts 
Valley, is one of disturbed sedimentary rocks. 

KINSNER SODA SPRING (MENDOCINO 14). 

Kinsner Soda Spring rises in a ravine 150 yards south of the wagon 
road and a mile west of Travelers Home. The water, which rises in 
a small basin excavated in soft sandstone, is strongly carbonated 
and probably contains considerable calcium, for hme carbonate and 
cemented gravel line portions of the bed of the ravine. At the road- 



CARBONATED SPRINGS. 175 

side there is a lime-carbonate mound 20 feet in diameter that was 
also probably formed by deposition from a former carbonated spring. 
Water from Kinsner Spring has been bottled and sold in WiUits for 
table use. 

CARBONATED SPRING ON WHITE RANCH (MENDOCINO 16). 

On the White ranch north of the road, about 1^ miles west of 
Kinsner Spring, there is another small carbonated spring. It has not 
been improved and is visited only by an occasional hunter or cattle- 
man. 

CARBONATED SPRING ON SNIDER RANCH (MENDOCINO 15). 

A short distance west of the White ranch there is a similar spring 
on the Snider ranch south of the road. It has not been improved 
and is known only locally. The same kind of sedimentary rocks that 
were noted farther east seem to form the hills in this neighborhood. 

CARBONATED SPRING SOUTHWEST OF WILLITS (MENDOCINO 19). 

In the mountains west of Wilhts Valley there are several minor 
carbonated springs which form drinking pools that are loiown mainly 
to hunters. One of these is in a ravine well up on the slopes, about 
10 miles by road and trail southwest of WilUts. The water here rises 
in a small triangular basin in the rock. It forms a good drinking 
pool, but, hke most of the springs of this kind, its yield is insignificant. 

CARBONATED SPRING WEST OF WILLITS (MENDOCINO 10). 

On the stage road to Mendocino, about 7 miles by road west of 
WiUits, there is a carbonated spring that is known to travelers over 
the route. Its water is cool and pleasantly carbonated, but its flow 
is slight. A small amount of iron is deposited along the run-off 
channel. 

CARBONATED SPRING IN BIG BASIN (MENDOCINO 9). 

About 15 miles west of Willits, in a timbered valley that is known 
as the Big Basin, there is a carbonated spring that is known mainly 
to lumbermen. Considerable amounts of iron stain its channel, but 
the yield of water is small. 

CARBONATED SPRINGS NEAR LONG VALLEY CREEK (MENDOCINO 8). 

In the canyon and tributary ravines of Long Valley Creek, about 
7 miles northward from Sherwood, there are a number of small 
mineralized springs. Several carbonated springs emerge within a 
space of 100 yards or more along the creek, two or three others are 
faintly sulphureted, and in one ravine carbonated water issues that 
deposits considerable iron. In 1910 none of tlie springs had been 



176 SPRINGS OP CALIPORISriA. 

improved except as drinking pools, but two camping and fishing re- 
sorts, known as Roses Range and Llewellyn Springs Camp, had been 
established in the vicinity. 

As in other portions of this region the rocks consist mainly of 
altered sediments. Near the iron-bearing springs, however, glauco- 
phane schist and float fragments of mica-garnet schist and pyroxene 
were noticed. 

JACKSON VALLEY MmERAL SPRINGS (MENDOCINO 6). 

Three springs issue close together on the southern bank of Mud 
Springs Creek, about 18 miles northwest of Sherwood. They are 
about 2 miles northeast of Branscomb post office in Jackson Valley 
and hence are locally known as Jackson Valley Mineral Springs. They 
rise in rock-walled basins from sandstone. The principal spring is 
moderately carbonated and also tastes distinctly alkaline, probably 
of soda. Some iron is deposited in the pool, whose discharge is perhaps 
2 gallons a minute. About three yards away there is a second basin 
of smaller discharge in which a greater amount, of iron is deposited. 
The third spring, about 4 yards farther downstream, is apparently 
little mineralized and discharges about 5 gallons a minute of cold 
water. 

Within recent years the property has been made a small camping 
resort, and water from the principal spring has been bottled and has 
found a local market. 

JACKSON VALLEY MUD SPRINGS (MENDOCINO 7). 

Three-fourths of a mile northeast of Jackson Valley Mineral Springs, 
on a knoll or bench on the northern side of the stream canyon, about 
200 feet above the creek, a group of mud springs have built up the 
small, well-formed craters shown in Plate XIII, A (p. 242) . The mud, 
which is light gray in color, covers a rudely circular area about 50 
yards in diameter. In its southern half there are five craters, 2 to 4 
feet high, but in 1909 only two of them had appreciable overflows. 
The largest one was about 5 feet in diameter and 4 feet high and dis- 
charged perhaps one-fourth of a gallon a minute of cool alkaline mud. 
In summer the mud is said to be covered by a deposit of efflorescent 
alkaline salts. The mud in the craters is kept in constant motion by 
bubbles of gas, which is probably carbon dioxide though its character 
was not definitely determined. The formation of the craters by mud 
which is probably brought up by a cool gas instead of by steam, as is 
usual in areas of mud volcanoes, is a unique feature of this locality. 
In a gully on the eastern side of the knoll water that is milky with 
suspended mud issues and forms a considerable stream. The rocks 
exposed in this gully indicate that the knoll is composed of crushed 
shale and sandstone, and this structure and topographic form of the 



CARBONATED SPRINGS. 177 

knoll suggest that it is a landslide mass. The place is visited as a local 
curiosity, but no attempt has been made to develop the springs in 
any way. 

CANTWELL SODA SPRING (MENDOCINO 5). 

In a ravine about a quarter of a mile north of Branscomb post office, 
on property that formerly belonged to a Mr. Cantwell, there is a small 
carbonated spring which has not been improved but has been used 
slightly as a drinking spring. Its mineralization, like that of a number 
of similar springs, is greatly diluted by surface water in the rainy sea- 
son, but in summer its water is said to be pleasantly carbonated. 

PETERSONS MINERAL SPRING (MENDOCINO 2). 

About 7 miles in a direct line east of north from Branscomb a small 
carbonated spring, that is known as Petersons Mineral Spring, rises 
at the edge of a small creek in an area of sandstone and conglomerate 
and has been protected by a rock wall and covered by a roof so as to 
form a drinking spring. Wlien visited it was flooded by surface 
water, but in summer its water is said to be moderately carbonated. 
Only a small iron stain was noticed near it and no other evidence of 
mineral deposits was seen, so it is probably a fairly pure water. 

The property has been a camping resort for several years. A 
small amount of the water was bottled and sokl for table use during 
one summer. 

WITTER MEDICAL SPRINGS (LAKE 16 j. 

Witter Medical Springs are situated 20 miles north of east from 
Ukiah, on a hillside that overlooks the vaUey at the northern end of 
Clear Lake. The principal sprmg at this place was used for its 
medicinal value by the Indians long before the settlement of the 
region by white people, and it has been known to the latter for more 
than 60 years. About 40 years ago the property was filed on by Dr. 
Witter, and a medical resort was gradually built up at the place. In 
the faU of 1900 the Witter Medical Springs Co. was incorporated, and 
a four-story hotel was opened in May, 1906. Several cottages provide 
accommodations for guests during the winter season, when the hotel 
is closed. 

The principal spring, which has long been known as Deadshot 
Spring, issues from crevices in massive rock at the creek edge in a 
ravine in front of the hotel and 250 yards from it by winding path. 
A small house protects the spring, which yields about five-eighths 
gallon a minute. The recorded temperature of the water is 53°. 
The water is strongly carbonated and noticeably saline in taste, and 
has been on the market as a medicinal water for a number of years. 
In 1910 the bottles were filled directly from the spring, corked, and 
35657°— wsp 338—15—12 



1Y8 



SPRINGS OF CALIPOENIA. 



conveyed by tramway to a warehouse a short distance down the ra vme, 
where they were labeled and boxed, and thence taken by team to the 
railroad at Ukiah. 

The following analysis shows the water to be highly concentrated 
and primary and secondary alkaline in character. The relatively 
large proportion of magnesium is of interest.^ 

Analysis of ivater from main spring at Witter Medical Springs, Lake County, Cal. 

[Analysts, Curtis and Tompkins (1902). Authority, advertising matter. Constituents are in parts per 

million.] 



Properties of reaction: 

Primary salinity 

Secondary salinity. . . 

Tertiary salinity 

Primary alkalinity. . . 
Secondary alkalinity . 
Tertiary alkalinity. .. 







S3 

39 

24 



Constituents. 



Sodium (Na) 

Potassium (K) 

Lithium (Li) 

Ammonium (NH4) 

Barium (Ba) and strontium (Sr). 

Calcium (Ca) 

Magnesium (Mg) 

Iron (Fe) 

Aluminum (Al) 

Manganese (Mn) 

Sulphate (SO4) 

Nitrate (NO3) 

Chloride (Cl) 

Carbonate (CO3) 

Metaborate (BO2) 

Phosphate (PO4) 

Silica (SiOz) 



weight. 



3,095 
84 
.04 
Trace. 
Traces. 
148 
950 

|- 4.9 

1.5 

8.6 

Trace. 

651 

6,032 

1.4 

.2 



11,060.64 



Carbon dioxide (CO2) 1, 166 



Reacting 
values. 



134. 53 

2.14 

.01 

Trace. 

Traces. 

7.43 

78.12 

.21 

.06 

.18 

Trace. 

18.36 

201.07 

.03 

.01 

2.77 



53.00 



About 25 yards upstream from Deadshot Spring another spring,, 
which is known as the Magnesia Spring but has been used only to a 
small extent for drinking, forms a shallow pool a foot in diameter 
at the base of a small bank and yields perhaps one-eighth of a gallon 
a minute of distinctly alkaline water. About 100 yards farther 
upstream the small Iron Tonic Spring issues at the edge of the creek, 
A concrete basin has been constructed around it and it has been used 
for drinking. Considerable iron is deposited on the gravel near this 
basin. Two miles westward, near the headwaters of the same 
drainage channel, there is a small sulphur spring, which has been 
used only to supply a cattle watering trough, but the plan of piping 
its water to the hotel grounds for drinking purposes has been con- 
sidered. A fifth spring, called Hummingbird Spring, near the 

1 Anderson (Mineral springs and health resorts of California, p. 266) gives an analysis of water from tliis 
spring which shows a solid content of only about 1,290 parts per million. The difEerences between his 
analysis and that more recently made, however, indicate that his analysis represents water from another 
spring. 



CAEBONATED SPRINGS. 179 

warehouse, which is in the ravine 100 yards below Deadshot Spring, 
issues through a pipe that has been set into the bank, and jaekls 
perhaps 3 gallons a minute of cool, fresh water that is used for a 
table supply at the hotel. 

The rocks of this locality seem to be the older sediments and 
associated metamorphics that compose the coastal ranges. Witter 
Hotel stands on shale and sandstone, and the usual more siliceous 
rocks that accompany these sediments are exposed eastward on the 
hillsides. Deadshot Spring emerges from a dark siliceous phase 
of the sandstone. About 30 yards southwest of the hotel, however, 
a ledge of serpentinous rock outcrops, and crosses the creek between 
the Iron Tonic and Magnesia springs. It forms the boundary between 
a small valley above it and the steep, narrow ravine below. Its 
relation to the Deadshot Spring and probably also to the Magnesia 
Spring suggests that it is the source of their unusually high magnesium 
contents. 

SARATOGA SPRINGS (LAKE 18). 

Saratoga Springs are on the side of a wide, brushy drainage ravine 
about 2 miles in a direct line southeast of Witter IMedical Springs. 
The property has been a resort since the seventies, and in 1910, 
accommodations for 250 people were provided by a hotel, annex, 
and 16 cottages, in an oak grove in a small flat along the creek. 

There are 12 small mineral springs on this property, 1 1 of them being 
on the slopes 100 to 150 yards east of the hotel. Six of these rise in 
cemented basins in a circular building 15 feet in diameter, known as 
the Roundhouse. They have been given such descriptive names as 
Appetizer and Digester. All are carbonated and deposit small 
amounts of calcium and iron, but they probably differ somewhat 
in the relative proportions of the solids in solution. Then- combined 
flow is perhaps H- gallons a minute. Ten yards southwestward 
there are two other similar springs, and 20 yards to the west there is 
one known as the Magnesia Spring. The water of the Magnesia 
Spring is less noticeably carbonated than that of the others, but it 
has a ferruginous taste and deposits considerable iron in its basin. 
About 50 yards south of the Roundhouse there is also a carbonated 
iron spring whose water deposits notable amounts of iron. In the 
bank near it there is a small exposure of lime carbonate and of iron- 
stained ocherous earth. All of the 10 springs thus far mentioned 
rise in cemented basins at the bases of small banks that expose 
crushed shale and sandstone. Their discharge is collected in a tank 
and supplies water for bathing. About 75 yards north of the Round- 
house a sulphur spring issues at the base of a bank of dark crushed 
shale. It yields peihaps 1 gallon a minute of strongly sulphureted 
water and because of its presence the locality is shown on Plate III 



180 



SPRINGS OF CALIFORNIA. 



as containing sulphureted-carbonated springs. The twelfth spring 
seeps from massive -sandstone two-fifths of a mile up the ravine from 
the hotel. Iron-stained lime carbonate is deposited by it on the rock 
face and indicates that the spring is similar in chemical character 
to the springs of the main group. 

The following analyses of fom springs at Saratoga show the water 
to be primary and secondary alkaline. The prominence of magnesium 
is an interesting chemical feature of the water. 

Analyses of water from Saratoga 8 frings, Lake County, Col. 
[Analyst, Selby Smelting Co. Authority, advertising matter. Constituents are in parts per million.] 



Properties of reaction: 

Primary salinity 

Secondary salinity. . 

Tertiary salinity 

Primary alkalinity. . 
Secondary alkalinity 
Tertiary alkalinity . 



117 



3 


7 
90 
120 



3 


11 

86 
147 



Constituents. 



By 
weight. 



React- 
ing 
values. 



By 
weight. 



React- 
ing 
values. 



By 
weight. 



React- 
ing 
values. 



By 
weight. 



React- 
ing 
values. 



Sodium (Na) 

Potassimn ( K) . . . 

Calcium (Ca) 

Magnesium (Mg). 

Iron ( Fe) 

Aluminum ( Al) . . 
Sulphate (SO4)..- 

Chloride(Cl) 

Carbonate (CO3). 
Silica (SiOz) 



180 

5.1 

270 . 

458 

5.8 

2.7 

Trace. 

55 

1,734 

105 



7.84 

.13 

13.48 

37.68 

.21 

.30 

Trace. 

1.54 

57.80 

3.48 



113 

4.3 

216 

421 

5.1 

2.8 

Trace. 

47 

1,478 

101 



4.90 

.11 

10.78 

34.63 

.18 

.31 

Trace. 

1.33 

49.27 

3.34 



111 

3.0 
147 
291 
3.6 
2.0 
4.1 
28 
1,063 
93 



4.83 
.08 

7.34 
23.94 
.13 
.22 
.09 
.79 
35.44 

3.10 



3.3 

117 

180 
3.6 
1.6 
5.3 
16 

708 



3.27 
.08 

5.86 
14.82 
.13 
.18 
.11 
.45 
23.60 

2.79 



2,815.6 



2,388.2 



1,745.7 



1,193.8 



Carbon dioxide (CO2) 1,439 



65.40 



1,250 



1,101 



50.00 



812 



36.91 



1,2,3,4. Separate springs, names not given. 

CARBONATED SPRING NEAR NORTHWEST EDGE OF CLEAR LAKE 

(LAKE 21). 

About 3 miles south of the town of Upper Lake a small carbonated 
spring rises in the alluvium near the lake edge, but it has not been 
improved and is little used. It forms a small, iron-stained pool that 
may be occasionally visited by a hunter or fisherman. 

CARBONATED WELL NEAR TIPPER LAKE (LAKE 19). 

In connection with the existence of the carbonated spring just 
described, two flowing wells in the locality, which yield noticeably 
carbonated water, may be mentioned. One of these is near the north- 
ernmost extension of Clear Lake, north of the carbonated spring, and 
is one-half mile south of the town of Upper Lake. It is situated on 
the Taylor place, is 2\ inches in diameter, and was sunk about 1905 
to a depth of 108 feet. In 1910 it yielded about 5 gallons a minute 
of cool, slightly carbonated water. It was used only for domestic 
purposes. 



CARBONATED SPRINGS. 



181 



CARBONATED WELL SOUTH OF UPPER LAKE (LAKE 20). 

About half a inile south of the Tayh)rw('ll (Lake 19, p. 180) thoro is 
another one, known as tlie Packwood well, wliich was sunk during 
the nineties to a depth of about 70 feet. It also yields carbonated 
water which may contain a notable amount of iron, for its run-off 
channel is deeply iron stained. It is more probable, however, that 
the iron comes from the well casing. Water from other wells at 
Upper Lake is said to contain mineral that quickly rusts tinned-iron 
vessels. 

CARBONATED WELLS AT KELSEYVILLE (LAKE 35). 

There is a group of carbonated wells in the eastern part of Kelsey- 
ville wliich may also be described in this connection. These wells 
were bored a nmnber of years ago on a low inound a quarter of a mile 
east of the business portion of Kelseyville and yielded much gas and 
carbonated water. The gas was formerly piped to buildings in the 
town for heating and lighting, but its use has been discontinued. 
Considerable gas and water still rise, and the latter is used for irriga- 
tion. The following analysis shows the water to be primary saline 
and secondary alkaline in character and to contain iron, aluminimi, 
and silica in unusually large amounts : 

Analysis of ivater/rom artesian well at Kelseyville, Lake County, Cal. 
[Analyst and authority, Winslow Anderson (18S9). Constituents are in pnrts per million.] 



Temperature 

Properties of reaction: 

Primary salinity 

Secondary salinity 

Tertiary salinity 

Primary alkalinity 

Secondary alkalinity 

Tertiary alkalinity 

Constituents 

Sodium (Na) 

Potassium ( K) 

Lithium (Li) 

Barium (Ba) 

Calcium (Ca) 

Magnesium (Mg) 

Iron ( Fe) 

Aluminum ( Al) 

Manganese ( Mn) 

Sulphate (SO4) 

Chloride (CI) 

Iodide (I) 

Carbonate (CO3) 

Metaborate (BOz)" 

Silica (SiOu) 

Carbon dioxide (CO2) 



24° C. (76° F.) 

50 


U 
39 
26 



weight. 



Reacting 
values. 



484 

36 
Trace. 
Trace. 

93 
111 

41 

47 
1.5 
639 
164 

10 
577 

23 
110 



2,336.5 



21.04 

.92 

Trace. 

Trace. 

4.64 

9.13 

1.47 

5.20 

.05 

13.31 

4.63 

.08 

19.23 

.53 

3.65 



82 



3.71 



a Reported as borates. Recalculated from NajBiO?. 



182 SPEINGS OF CALIFORNIA. 

LEE SODA SPRING (LAKE 31). 

There is a small unbuproved carbonated spring on tlie Lee ranch 
in the canyon of Scott Creek about 4 miles in a direct line southwest 
of Lakeport. Its water is cool and moderately carbonated, but the 
place is rather inaccessible and is seldom visited. 

CARBONATED SPRING IN CANYON OF SCOTT CREEK (LAKE 30). 

About 1^ miles west of the Lee spring there is another carbonated 
spring in the canyon of Scott Creek, also small in flow, unimproved, 
and seldom visited. Similar springs, which are known only to hunt- 
ers, probably rise at other places in this region. The rock formations 
consist of the same series of sedimentary materials that was observed 
through the gTeater part of the coastal ranges in the north-central 
section of the State. 

GLEN ALPINE SPRINGS (LAKE 33). 

At Glen Alpine Springs, on the western bank of Scott Creek, 6 
■ miles southwest of Lakeport and beside the wagon road between that 
town and Hopland, two small springs rise in bricked and cemented 
basins about 4 yards apart. A road house near the springs was for- 
merly kept open, but of late years the place has been deserted. The 
water is moderately carbonated, but when visited in 1909 there was 
no overflow. Small amounts of iron have been deposited on the 
basin sides, and at the creek edge 5 yards away a very hard deposit 
of lime carbonate a foot thick is exposed for a few yards. The coun- 
try rock, which is well shown along the road near by, consists of the 
usual series of shale and sandstone. 

BYNUM SPRING (LAKE 34). 

Bynum Spring is situated a mile south of Glen Alpine Springs, in 
a small ravine that is tributary to Scott Creek. Its water rises from 
crushed sandstone near the edge of the stream channel, in a cemented 
pool about the size of a barrel. When visited in 1909 there was no 
overflow. The water was strongly carbonated, and slight deposits 
of lime carbonate and iron had formed in the basin. The water has 
been bottled at the spring and marketed locally as a table water. 
The following analysis shows that it is essentially a secondary alkaline 
water. 



CARBONATED SPRINGS. 



183 



Analysis of ivalcr from ByiiumS pring, Lake County, C'al. 
[Analyst, F. T. Green (1909). Authority, owner of spring. Constituents are in parts per million.] 



Properties of reaction: 

Primary salinity 

Secondary salinity 

Tertiary salinity 

Primary alkalinity 

LSecondary alkalinity 

Tertiary alkalinity 

Constituent 

Sodium (Na) 

Calcium (Ca) 

Magnesium (Mg) 

Iron(Fe) 

Sulphate (SO4) 

Chloride (CI) 

Carbonate (CO3) 

Silica (SJO2) 

Carbon dioxide (CO2) 



(?) 



By 
weight. 



Reacting 
values. 



16 

333 

173 

2.2 

30 

2.9 

928 



.70 
16.62 
14.23 



30.93 
2.95 



1,574.1 



Present. 



Present. 



HIGHLAND SPUINGS (LAKE 39). 

The property at Highland Sprmgs has been improved as a resort 
for 25 years or more. It is situated on the stage road between Hop- 
land and Kelseyville and 6 miles southwest of the latter place. In 
1910 a large frame hotel and half a dozen cottages situated in a small 
flat along the course of Adobe Creek provided accommodations for 
200 guests. 

Eleven springs, or 10 individual springs and 1 group, may be 
recognized here. One of these, the Seltzer Spring, emerges at the 
base of a gentle slope about 150 yards southeast of the hotel. The 
others issue west to northwest of the hotel in a distance of about 
225 yards along the western bank of the creek. Seltzer Spring, which 
is protected by a latticed spring house, rises in a cemented basin; 
the recorded temperature of the water is 59° and its discharge is 
perhaps 1 gallon a minute. The water is strongly carbonated and 
deposits considerable iron. 

Neptune Spring, the southernmost of those along the creek, is 
about 100 yards west of the hotel. The spring rises in a small drink- 
ing pool in the center of an oval cemented basin, several feet across, 
on a gentle slope at the base of a low bank. The water has a re- 
corded temperature of 66°. Its flow is slight, but it is piped to a 
small bathing plunge a few yards away. At the base of a smaU bank 
50 or 60 yards northward and nearer the creek, Diana Spring and 
Magnesia Sprmg rise in cemented basins a few yards apart. Water 
from the former supphes a small bathing plunge near by, whereas the 
lattc- is used only for drinking. The recorded temperatures of these 
springs were 80° and 68°, and their flows were, respectively, about 4 



184 SPRINGS OF CALIFORNIA. 

gallons and one-fourth gallon a minute. From about 30 to nearly 55 
yards beyond the Magnesia Spring much water rises beneath a platform. 
This water supphes an adjacent bathhouse and is also piped across 
the creek to a swimming plunge. Temperatures of 72° to 82° were 
recorded at different points beneath the platform. The discharge, as 
nearly as it could be estimated, is about 10 gallons a minute. There 
are two small pools with slight overflow along .the creek bank a few 
yards north of the bathhouse and an iron-stained seepage area extends 
about 10 yards along the creek edge. Beyond this area there is a small 
board-curbed pool which discharges about 2 gallons a minute of 
water 73° in temperature. Ten yards beyond, at the northern end 
of the line of springs, Arsenic and Dutch springs rise in separate 
compartments of a circular, cemented basin near the creek edge. 
Their recorded temperatures were, respectively, 68° and 72°. Ar- 
senic Spring yields approximately one-half gallon a minute and 
Dutch Spring perhaps twice as much. 

All the springs are carbonated, and their basins are stained by 
iron. Small amounts of hme carbonate are deposited at several 
places, and south of the springs, along the road westward from the 
hotel, a deposit of lime carbonate several feet thick is exposed for 
50 yards or more. The springs seem to issue mainly from crushed 
sandstone and shale, but along the northern part of the bank from 
which they come forth slickensided, apparently serpentinized mate- 
rial is exposed. The temperature of the water suggests that crushing 
and other movements have here taken place and have given rise 
to the springs. The locaHty is shown on the map (PI. Ill, in pocket) 
as one of thermal carbonated springs, but the springs are known chiefly 
for their carbonated waters, which the following analyses show to be 
essentially secondary alkaline in character. 



CARBONATED SPRINGS. 



185 



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186 SPRINGS OF CALIFORNIA. 

ENGLAND SPRINGS (LAKE 40). 

Eight miles south of Kelseyville a number of small carbonated 
springs issue near a road that was formerly the main road to Clover- 
dale by way of The Geysers (Sonoma 4, p. 83). This road follows up 
Adobe Creek for several miles, but it has been unused for a number 
of years. In 1910 the property near the springs was abandoned or 
used only as a goat range. 

The springs are locally known as England Springs, after the name 
of the first locator or owner, though on some maps they are named 
Elliott Springs, after a later owner. One small carbonated spring 
issues from a bank of shale near the road and opposite the house on 
this property. A ravine enters Adobe Creek from the southeast at a 
point 150 yards down the road, northeast from this spring. Along 
the sides of this ravine and 250 to 300 yards from the road, are six 
other small springs that have been excavated to form drinking pools, 
two of which have been chiefly used by picnic parties. In one of the 
springs a temperature of 76° was measured, and as the water of the 
others is also noticeably above a normal temperature, the locality is 
indicated on Plate III as one of thermal carbonated springs. The 
flow of the springs ranges from about half a gallon to 1 gallon a minute. 
The waters are moderately carbonated and have deposited con- 
siderable iron as well as small amounts of lime carbonate. 

There are numerous small iron-stained lime carbonate deposits at 
seepages from fissures in the rock along the edge of Adobe Creek, 
one-half to three-fourths mile below England Springs, but no flowing 
springs were noticed. The rocks of the locality comprise the usual 
series of crushed shales and sandstones and are well exposed along 
the canyon of Adobe Creek. 

CARBONATED SPRINGS ON COLE CREEK (LAKE 42). 

Near the road between Kelseyville and Middletown and 4^ miles 
south of the former place two carbonated springs rise near the channel 
of Cole Creek. Around one of these, which issues at the eastern edge 
of the creek, a cemented basin, 6 feet in diameter, has been con- 
structed. Much gas rises in it, and the water deposits considerable 
iron. The spring had apparently been improved as a drinking basin 
in the grounds of a smaU residence that stood near by, but when 
seen the property was deserted. The second spring rises about 
75 yards downstream from the main spring and on the opposite side 
of the creek, some distance from its bank. It has been protected by 
a smaU board curbing, and also deposits considerable iron. Both 
springs are of small flow and apparently have been used only for 
drinking. 

The rock here seems to consist of a thin layer of obsidian gravel 
that overlies lake sediments. The gas that is given off from the main 
spring may be similar in composition to that of the gas weUs at 
KelseyviUe (p. 181). 



CARBONATED SPRINGS. 



187 



CARLSBAD SPRINGS (LAKE 41). 

Carlsbad Springs are also situated along Cole Creek, half a mile 
south of those that have just been described but farther upstream, 
where the creek flows in a brushy ravine. The property was con- 
ducted as a small resort for several years prior to 1905, but it has been 
deserted since about that year, and in the summer of 1908 a brush 
fire destroyed the hotel building. 

Five springs on tliis property rise along the western side of the 
ravine within 100 yards of the hotel site. The principal one seems 
to have been that known as the Arsenic Spripg, wliich rises in a semi- 
circular, rock-walled place on the slope 50 yards southwest of the 
creek. The recorded temperature of the water in this spring is 74° 
and the yield is about one-fourth gallon a minute of carbonated 
water. Ten yards below it is a similar spring in which the water has 
nearly the same temperature, but wliich yields perhaps 2 gallons a 
minute. Water from this spring was formerly piped to a small bath- 
house at the opposite side of the creek. A third spring rises near the 
creek in a rock-walled basin 8 feet in diameter, but it has no surface 
overflow. Another spring rises 60 yards farther downstream, at the 
edge of a small marshy area. It has a temperature of 66° and a flow 
of at least 2 gallons a minute. Iron-stained seepages issue beside the 
bathhouse and also 125 yards downstream from it, but the lower 
seepages do not appear to have been improved. 

The following analyses of springs at this place have been published 
and are reproduced in standard form, but the spring to wliich each 
applies was not identified : 

Analyses of water from Carlsbad Springs, Lake County, Cal. 

lAnalvst, W. D. Johnston. Authority, Register of Mines, California Min. Bur. Constituents are in parts 

per million.] 



3 



Temperature 

Properties of reaction: 

Primary salinity 

Secondary salinity. . . 

Tertiary salinity 

Primary alkalinity . . 
Secondary alkalinity. 
Tertiary alkalinity. . . 



30°C.(85°F.). 




7 
93 
763 



24°C. (75°F.). 




12 

88 
788 



27"C. (80°F.). 




21 
79 
1,532 



27°r. (S1°F.). 



946 



25°C.(77°F.). 




9 
91 
736 



Constituents. 



By 

weight. 



React- 
ing 

values. 



By 
weight. 



React- 
ing 
values. 



By 
weight. 



React- 
ing 
values. 



By 

weight. 



React- 
ing 
values. 



By 
weight. 



React- 
ing 
values. 



Sodium (Na) 

Potassium (K).. 

Lithium (Li) 

Calcium (Ca) 

Magnesium (Mg) 

Iron(re) 

Aluminum (Al). 
Carbonate (CO3) 
Silica (SiOz) 



Carbon dioxide (CO2) . . . 



14 
4.7 
Trace. 
13 
102 
1.5 
1.1 
294 
Trace. 



0.61 

.12 

Trace. 

.65 

8.38 

.05 

.12 

9.79 

Trace. 



23 
3.4 
Trace. 
24 
SO 
.1 
1.4 
266 
Trace. 



1.00 

.09 

Trace. 

1.20 

6.58 

Trace. 

.16 

8.87 

Trace. 



15 
5.9 
Trace. 
11 
30 
.1 
1.0 
115 
Trace. 



0.65 

.15 

Trace. 

.55 

2.47 

Trace. 

.11 

3.82 

Trace. 



20 
3.4 
Trace. 
20 
72 
.9 
1.1 
237 
Trace. 



0.87 

.09 

Trace. 

1.00 

5.92 

.03 

.12 

7.91 

Trace. 



17 
3.6 
Trace. 
14 
92 
.1 
1.6 
272 



0.74 

.09 

Trace. 

.70 

7.54 

Trace. 

.18 

9.07 



430.3 



397. 9 



178.0 



354. 4 



400.3 



1,720 



1,537 



69.86 



1,287 



1,645 



1,569 



71.32 



1, 2, 3, 4, 5. Separate springs, names not given. 



188 



SPEIlSrGS OF CALIFORNIA. 



The analyses indicate that the spring waters are secondary alka- 
line in character with very high tertiary alkalinity and a notable degree 
of primary alkalinity. The fact that sulphate and chlorine radicles 
are not included and that silica is reported as only a trace renders 
these analyses of doubtful reliability. 

Like other springs yielding notably thermal carbonated water Carls- 
bad Springs are marked on Plate III (in pocket). The slopes at the 
springs are covered with lava that is probably andesite. For a 
short distance along the road grade, 1 or 2 miles southward and a few 
hundred feet higher, however, fine-bedded sediments that are similar 
to the lake beds near Kelseyville are exposed. At other places in 
this portion of the county the lava also appears to be present as a 
thin layer overlying sedimentary material. 

ASTORG SPRDTG (LAKE 45). 

A number of years ago a short prospect tunnel was run into the 
hiUside three-quarters of a mile south of east from Glenbrook post 
office, which is 30 miles north of Calistoga. After the tunnel had 
been abandoned as a mining enterprise, the character of the water in 
it was noticed, and for a short time the water was shipped in tanks 
to San Francisco, carbonated, and bottled as a table water. When 
seen in 1910, however, the property was deserted. A reservoir had 
been formed in the tunnel by an earth and board dam across it. 
Although shghtly carbonated, the overflow, perhaps one-eighth gal- 
lon a minute, seemed to be mainly of surface origin, and the rela- 
tively small mineral content of the spring water, as shown by the 
following analysis, tends to confirm the belief that it is essentially 
a surface water. The analysis, which is not complete and does not 
appear to be very reliable, indicates a secondary alkaline and 
primary saline water. 

Analysis of water from Astorg Spring, Lake County, Cal. 

[Analyst, M. E. Diebod. Authority, Register of Mines, California Min. Bur. Constituents are in parts 

per million.] 



Temperature 

Properties of reaction: 

Primary salinity 

Secondary salinity. . . 

Tertiary salinity 

Primary alkalinity. . . 
Secondary alkalinity. 
Tertiary alkalinity. . . 



10° C. (50° F.) 




Constituents. 



Sodium (Na) 

Potassium ( K) . . . 

Calcium (Ca) 

Magnesiimi (Mg). 

Iron (Fe) 

Manganese (Mn) . 
Sulphate (SO4)... 
Carbonate (CO3) . 
SiUca (SiOs) 



CARBONATED SPRINGS. 



189 



The tunnel is in an area of serpentine that is hero associated with 
sedmientary rocks and is overhiin on the hill slopes above by lava. 

It is locally known as the Tunnel Spring, and its water is called a 
"chamise" water, as it is thought by some persons to taste of the 
chamiso brush roots. Another small carbonated spring of even less 
importance rises in Sulphur Valley, 1 or 2 miles north of Astorg 
Spring. 

ADAMS SPRINGS (LAKE 44). 

Adams Springs are situated in a deep ravine about 2 miles eastward 
across a divide from Astorg Spring. The springs are said to have 
been found and filed on by a Mr. Adams more than 40 years ago. The 
property has been improved as a resort for more than 20 years, but it 
has attained prominence chiefly since about 1900. A large drain 
pipe has been laid in the stream channel to carry off storm water, and 
the ravine has been widened and leveled to obtain space for buildings. 
In 1910 a large frame hotel and a number of cottages and tents fur- 
nished accommodations for about 400 people. A swimming plunge 
on the hillside above the springs is supplied by water piped from a 
stream. Though the water is used by some people for its medicinal 
value, the place is essentially a summer pleasure resort. 

Analyses of water from Adams Springs, Lake County, Cal. 
[Constituents are in parts per million.] 



Properties of reaction: 

Primary salinity 

Secondary salinity. . . 

Tertiary salinity 

Primary alkalinity. . . 
Secondary alkalinity. 
Tertiary alkalinity. . . 



2 


26 
72 
156 



2 


26 

72 
175 



Constituents. 



By 
weight. 



Sodium (Na) 

Potassium (K)... 

Calcium (Ca) 

Magnesium (Mg). 

Iron(Fe) 

Aluminum (Al).. 
Sulphate (SOO... 
Nitrate (NO3).... 

Chloride (CI) 

Carbonate (CO3). 
Silica (SiOo) 



441 

Trace. 

199 

483 

4.6 

Trace. 

17 



48 

2,019 

127 



3,338.6 



Carbon dioxide (CO2) J 2, 261 



Reacting 
values. 



By 

weight. 



19.18 

Trace. 

9.93 

39.73 

.16 

Trace. 

.35 



454 

Trace. 

197 

488 

4.3 



1.35 

67.30 

4.21 



Trace. 

44 

2,059 

124 



3,370.3 



102. 77 



Reacting 
values. 



19.74 

Trace. 

9.83 

40.15 

.15 



Trace. 

1.24 

68. 63 

4.11 



1. Mainspring. Analyst and authority, Winslow Anderson (1888). 

2. Main spring. Analyst, Price and Hewston. Authority, U. S. Geol. Survey Bull. 32. 



The main spring, which is situated a few yards above the hotel and 
close to the former channel of the ravine, is inclosed by a frame build- 
ing, and the water is dipped from a small pool for drinking, but it is 



190 SPRINGS OP CALIFORNIA. 

also piped to a bottling house below the hotel. It is used on the 
grounds only for drinking and is bottled for table use. The water is 
cool — a temperature of 46° being recorded in tlie spring in January, 
1910, but it is probably about 55° in summer — and the yield is per- 
haps one-half gallon a minute. It is strongly carbonated and has a 
petroleum odor and taste similar to th^.t which was noticed at Skaggs, 
Gordon, and Seigler springs. The analyses on page 189 show it is 
a secondary alkaline water with notable primary alkalinity and high 
tertiary alkalinity. 

A smaller spring, the water of which is similar in character to that 
of the main one, issues from the bank opposite the latter but has not 
received much attention. 

The rocks exposed along the ravine are sandstones and shales 
which dip steeply, but the structure shown is probably to a large 
extent of landslide character. On the higher slopes near the springs 
these sediments are overlain by basaltic or andesitic lava. 

BONANZA SPRINGS (LAKE 50). 

Bonanza Springs are situated in a grove on a gentle slope border- 
ing a ravine, about 3 miles north of east from Adams Springs, and 
halfway between Seigler and Howard sprmgs (described among the 
hot springs, pp. 95-98). The property has been a camping resort for 
a number of years. In 1910 there were 8 or 10 small cottages and 
grounds for tents near by. 

Three springs, which are known as Sulphur, Soda, and Iron, are 
situated on the property. The Sulphur Spring is in a covered well, 
9 feet deep, from which a pipe extends a few yards northeastward 
down the slope to a latticed house, where the water issues from a 
small jet. This water is cool and noticeably sulphureted and also 
has a slight oily odor and taste. An oily film is said to form on the 
water of a shallow well near by. The Soda and the Iron springs 
issue a few feet apart from crevices in a smaU exposure of sandstone 
60 yards below the Sulphur Spring house. Both are cool and car- 
bonated and have stained their basins with iron, though the Iron 
Spring has done so to the greater extent. All three springs are small, 
yielding only one-quarter to one-half gallon a minute each. 

The rock at this locality seems to be sandstone, but on the slopes 
a short distance above it is overlain by lava. 

SPIERS SPRINGS (LAKE 62). 

Spiers Springs are situated about 3 miles in a direct line southeast 
of Bonanza Springs, in the canyon of the main branch of Putah 
Creek. 

Two springs of similar character issue a few yards apart at this 
place and each discharges 7 or 8 gallons a minute. The water is 
moderately carbonated and is noticeably sweet, probably from mag- 



CARBONATED SPEINGS. 191 

nesia. Tlieir overflow channels are iron stained. One of the springs 
issues at the base of a serpejitine bank on the eastern side of 
the creek channel and has been piped to the creek edge. Its water 
has been bottled for sale since about 1901. The other spring issues 
from crevices m serpentine at the eastern edge of the creek. The 
water seems to be similar in chemical character to that of the firet, but 
in 1910 the spring was unimproved. 

Although no analyses of these sprmgs are available, the close rela- 
tion of magnesia content to serpentme from which the water issues 
is thought to be well show^n at these springs, as at other magnesia 
springs that have been described. 

The canyon of this branch of Putah Creek seems to mark the 
western boundary of the serpentine near Spiers Springs, for though 
it covers an extensive area on the eastern side of the canyon, the banks 
on the opposite side are of sedmientary rocks. 

Spiers Springs are noticeably thermal, temperatures of 74° and 78° 
havmg been recorded, so they are shown on Plate III (in pocket) as 
thermal-carbonated springs, but they seem to be more properly con- 
sidered as carbonated springs. There is said to be another magnesia 
sprmg, though of only slight flow, known as Sweetwater Spring, 2 or 3 
miles southeast of Spiere Springs, but it has been unused and was not 
found. 

SODA BAY SPRINGS (LAKE 36). 

Soda Bay Sprmgs are situated at the western side of Clear Lake,, 
near the north base of Mount Konocti, a lava peak that rises high 
above the lake. A boating and fishmg resort has been established 
here for nearly 40 years, and in 1910 a hotel and cottages provided 
accommodations for about 150 people. 

Numerous warm, bubbling springs rise along the border of the lake 
for a distance of half a mile on the east side of the bay, but five princi- 
pal sprmgs and groups may be recognized. Two of the springs are 
respectively about 200 and 235 yards east of the boat pier. They 
form carbonated drinking pools having temperatures of 90° and 82°. 
In January, 1910, they were at the lake edge, but as the lake surface 
fluctuates several feet during the year, the springs are sometimes 
submerged. All of the vents are said to be more active when the 
lake is high. From the two springs already mentioned, a line of 
bubbles extended northward about 300 yards, parallel with the 
lake edge but several yards out from shore, to a float that was used 
by bathere. A group of small vents here made the water warm and 
pleasant for bathing. At a low point 250 yards farther northwest, 
small flows of carbonated water 85° to 90° m temperature issued from 
iron-stained cemented gravel, both on the shore and for several yards 
mto the lake. The lai'gest and most unportant sprmg, however, rises 
in tlie lake 200 yards or more northwest of the spi-mgs last described 
and near the northern end of a small island. This spring is known as 



192 



SPRINGS OF CALIFORNIA. 



the Geyser Spring, or Omar-Ach-Hah-Bee, the Great Spruig, and m 
July, 1910, it had a temperature of 87°. Its flow was not measurable 
but is probably several hundred gallons a minute, and much water 
also rises at other points near by. A dressing room has been built 
on the lake over this spring, which rises in a pit in an inclosure, and 
the place is used for bathing. The analysis shows the water to be 
distinctly ferruginous in character — a fact that is also evidenced by 
the iron stains on the adjacent rocks. It is a secondary-alkaline water 
with notable prunary alkalinity. 

Dr. Wmslow Anderson ^ mentions a hot borate spring near the shore 
of Clear Lake, which in July, 1888, had a temperature of 124° and 
yielded 300 gallons a mmute. The description given apparently 
refers to the Geyser Spring, but the difference in temperature is rather 
large, and the analyses he quotes vary so widely from the analyses 
made in 1910 that it seems probable that different springs were 
sampled. The Hot Borate Sprmg of Anderson is a primary alkaline 
water of high concentration with notable primary salinity. The 
prominence of ammonium and metaborate radicles is noteworthy. 
The analyses of both springs are reproduced herewith. 

Analyses of water from Soda Bay Springs, Lake County, Col. 
[Constituents are in parts per million.] 



Temperature 

Properties of reaction: 

Primary salinity 

Secondary salinity . . . 

Tertiary salinity 

Primary alkalinity. . . 
Secondary alkalinity. 
Tertiary alkalinity. . . 



31° C. (87° F.) 



(?) 



32° C. (88° F.) 





17 
74 
250 



51°C.(124°F.) 

26 



74 

Trace. 

29 



27 



73 
Trace. 

36 



Constituents. 



By 

weight 



Sodium (Na) 

Potassium (K) 

1/itliium (Li) 

Ammonium (NH4) 

Barium (Ba) and strontium (Sr). 

Calcium (Ca) 

Magnesium (Mg) 

Iron (Fe) 

Aluminum (Al) 

Manganese (Mn) 

Sulphate (SOO 

Nitrate (NO3) and nitrite (NO2).. 

Chloride (Cl) 

Bromide (Br) 

Iodide (I) 

Carbonate (CO3) 

Metaborate (BO2) 

Arsenate ( AsO^) 

Phosphate (PO4) 

Silica (SiOo) 



115 
9.5 



85 
113 



Trace. 

"eo" 



16.00 
Present. Present 



React- 
ing 
values. 



By 

weight 



5.00 

.24 



4.24 
9.30 

.82 



Trace. 

'"{'.Yq 



Trace. Trace. 
132 4.38 



104 
12 

.5 
2.6 
.0 
92 
118 
f 6.1 
I .8 
1.0 
.2 
.0 
60 
.0 
Trace. 
529 
1.6 
Trace. 
Trace. 
142 



1,022.3 



1,069.8 



Carbon dioxide (CO2) ■. 963 



React- 
ing 
values. 



By 
weight. 



4.52 

.32 

.08 

.14 

.00 

4.60 

9.72 

.22 

.08 

.03 

Trace. 

.00 

1.68 

.00 

Trace. 

17.64 

.04 

Trace. 

Trace. 

4.70 



1,722 
29 



376 



Trace. 
2.1 



19 
.Trace. 



897 
Trace. 
1.6 
1,112 
1,471 



136 



5, 765. 7 



43.77 



527 



React- 
ing 
values. 



By 
weight. 



74.84 
.74 



1,547 
Trace. 



Trace. 
.17 



Trace. 
.1 



2.05 
Trace. 



11 
Trace. 



25.30 

Trace. 

.01 

37.07 

34.20 



879 
Trace. 
1.4 
1,171 
1,152 



141 



5,323.5 



23.96 



622 



React- 
ing 
values. 



67.26 
Trace. 



23.36 



Trace. 
.01 



1.27 
Trace. 



24.80 

Trace. 

.01 

39.02 

26.80 



1. Geyser Spring. Analyst and authority, F. M. Eaton (1910). 

2. Geyser Spring. Analyst and authority, Curtis and Tompkins (1910). 

3. Hot Borate Spring. Analyst and authority, Winslow Anderson (1888). 

4. Hot Borate Spring. Analyst, Moore; authority, Winslow Anderson. 



1 Mineral springs and health resorts of California, p. 176. 



CARBONATED SPRINGS. 193 

CARBONATED SPRINGS AT SOUTHWEST EDGE OF CLEAR LAKE (LAKE 37). 

About 5 miles southeastward around the west side of the lake from 
Soda Bay small warm carbonated springs issue for a distance of 25 
yards along the lake margin. A quarter of a mile farther south 
numerous other springs rise within a stretch 200 yards long. One of 
the largest noted had a temperature of 100° and a flow of perhaps 
1 gallon a minute. Its water was moderately carbonated and also had 
a noticeably "sharp " taste that was possibly due to free carbonic acid. 
At both of the localities mentioned there is considerable iron-stained 
cemented gravel and sand. 

The rock that is exposed from about 2 miles west of Soda Bay, 
eastward and southward around the lake to and beyond the springs 
just described, is the andesite of Mount Konocti. There appears to 
be a close relation between the numerous warm carbonated springs 
and this comparatively recent lava. The thermal character of the 
springs at Soda Bay and farther southeast has been noted in the 
description of the springs at Sulphur Bank (p. 99). Their carbonated 
character is also noteworthy in connection with the presence of the 
lava. This association of lava with carbonated springs at several 
places has already been mentioned, and it is brought out in the tabu- 
lated arrangement of the carbonated springs (pp. 250-253). 

BAKER SODA SPRING (LAKE 53). 

A small carbonated spring, knowii as Baker Soda Spring, lies 
about halfway between Lower Lake and Reiff post office. Its water 
has been used to small extent for drinking, but in 1910 it had not 
been commercially developed and was of only local interest. Like 
most of the other carbonated springs in Lake County, it issues from 
sedimentary rocks, probably of pre-Cretaceous age. 

GRIZZLY SPRINGS (LAKE 29). 

Grizzly Springs (PI. XIII, B, p. 242), w^hich have also been kno\^^l 
as Richardson Springs, issue on the northern side of Grizzly Canyon, 
about 2J miles above its junction wdth Cache Creek. As the si)rings 
are beside a main road that leads up the canyon and across the 
divide into Colusa County, they have been kn(n\ai for many years, but 
they have been improved only since about 1908. 

There are two springs on the property. The Main Spring has 
formed a prominent carbonate deposit that extends down to the 
creek and is crossed by the road. The water rises with continual 
bubbling in a cemented rock-walled pool beneath a shed roof and 
yields about 2 gallons a minute of moderately carbonated and notice- 
35657°— wsp 338—15 13 



194 SPRINGS OF CALIFORNIA. 

ably sulphureted, salty water. ^ The pool is used as a drinking basin, 
and a pipe leads from it to a heating tank a few yards away and thence 
to a small bathhouse. Besides its use by campers for bathing, the 
water has been bottled and sold locally. 

In two or three places a few hundred yards farther upstream there 
are small lime-carbonate deposits where carbonated water evidently 
issued at a former period. The second spring, which is called the 
Arsenic Spring, flows from a small pit dug in a grassy seepage area 
on the hillside about 175 yards northwest of the Main Spring. It 
yields perhaps one-half gallon a minute of salty magnesic water and 
has been used for drinking. 

A small amount of serpentine is exposed near the Arsenic Spring 
and probably furnishes the magnesic contents of both springs. 
Well-bedded sandstones and shales that continue up the canyon 
beyond the spring probably furnish the other mineral constituents. 
Cemented gravels belonging to the beds described by Becker ^ as the 
Cache Lake beds, of late Pliocene age, extend up the canyon approxi- 
mately to the springs. The springs apparently issue at the eastern 
limit of the gravels, though conclusive evidence of this was not seen. 

OIL SPRING (COLUSA 8). 

Prominent deposits of lime carbonate have been formed on the 
steep hillside that borders the western side of Bear Valley, about 1| 
miles north of Wilbur Hot Springs (Colusa 9, p. 99), These deposits 
extend for about one-quarter of a mile along the hillside and 200 to 
300 feet above Bear Creek. At three or four places there are seepages 
of salty, carbonated water, but the main flow is at the northern and 
largest deposit. Here a spring that is locally called the Oil Spring 
yields about 2 gallons a minute of water, 76° in temperature, that 
tastes salty and disagreeably of petroleum. A number of years ago 
a shed was built over the spring, a collecting tank for the oil was 
placed near by, and a pipe line was laid to two large storage tanks in 
a shed beside the creek. In 1910 these improvements still remained, 
but the attempt to collect oil in commercial quantity from the spring 
had proved unsuccessful. A well that was drilled for oil a few miles 
north of the spring was also unsuccessful in obtaining a supply. 

The spring and associated seepages issue from shales and sand- 
stones that here border Bear Valley and extend eastward to Sacra- 
mento Valley. These sediments are relatively unaltered, compared 
with the sediments of the Franciscan formation, but a portion of 
them may belong to the Knoxville formation (Lower Cretaceous) . 

1 An analysis of this water, indicating a mineral content of about 1,100 parts per million, -with rather 
low sodium and magnesium and unusually high lithium, has probably been incorrectly reported. 

2 Becker, G. F., Geology of the quiclcsilver deposits of the Paciflc slope: U. S. Geol. Survey Men. 13, pp. 
219-221, 1888. 



CAKJiois'ATEU spm^'(;8. 195 

DEADSHOT SPRINGS (COLUSA 6i. 

Uoadsliot Sprini^is arc sitiuilcd aloni^ a ravino wlios.^ mouth ia about 
one-half niik> aoutli of the buildmgs on the Stovall and Wilcox horse 
ranch in Boar Valley and about 5 miles southwest of Leesville. The 
])rincipal spring issues from a short piece of pipe inserted near the 
base of a lime carbonate terrace on the south side of the ravine, 
about 1 mile above its moutli. The top of the terrace extends for 
about 50 feet along the ravine, and tlie material exposed in its front, 
which is perhaps 20 feet high, indicates that the terrace is composed 
largely of serpentine fragments cemented by lime carbonate. 

The spring yields about 1^ gallons a minute of carbonated salty 
water, 65° in temperature, that is an active cathartic. About 150 
yards eastward, below the main spring, a flow of perhaps 6 gallons a 
minute of mildly carbonated, salty water issues on the south bank of 
the ravine. The water here comes from one main spring and several 
seejDages from carbonate-crusted patches in a small salt-grass area. 
On the north bank of the stream, 300 yards farther down the ravine, 
there is a carbonate terrace about 25 feet long and 1 feet wide. A 
small pool on its top yields about 1 gallon a minute of carbonated 
salty water, 78° in temperature. The material of part of the terrace 
is so deeply iron stained that it has an ocherous appearance. The 
lowest springs are about 150 yards farther downstream, on the north 
edge of the creek, and issue from two crevices about 6 yards apart. 
They yield flows of about a quarter of a gallon and 2 gallons a minute 
of water that is similar in character to that of the other springs. 

All these springs issue from serpentine, which here forms a wide 
belt that extends fi^om the valley land westward nearly or quite to 
the summit of the mountains and is possibly the northward extension 
of the serpentine area at Wilbur Hot Springs. It is Av^orthy of note 
that though Deadshot Springs issue from serpentine, and Oil Spring 
(Colusa 8, p. 194) a few miles farther south, issues from shale, both 
groups of springs yield carbonated salty water and have formed large 
carbonate deposits. 

QUIGLEY SODA SPRINGS (LAKE 27). 

Three carbonated springs that emerge about a quarter of a mile 
from each other on the Quigley place, 14 miles by road north of the 
town of Lower Lake, have been surrounded by coiicrete basins so as 
to form drinking pools. One of them is near the western side of Long 
Valley Creek and apparently issues from siliceous shales that are over- 
lain by basaltic lava which forms a low ridge. The second spring is 
farther northwest, on the wooded slope of the lava ridge but close to 
the northern edge of the lava. The tliird s])ring is still farther to the 
northwest and issues at the side of a small ravine from a seam in 



196 SPRINGS OF CALIFORNIA. 

siliceous sandstone. Each spring yields one-half to 1 gallon a minute 
of moderately carbonated water, 60° to 65° in temperature, and heavily 
stains its overflow channel with iron. The water of the northern- 
most spring tastes noticeably of salt. The position of the springs 
near the northern border of the lava area is worthy of note and also 
their occurrence near cold fresh-water springs (Lake 28, p. 358), which 
are not common in this region. 

DESrSMORE SODA SPRING (LAKE 24). 

A carbonated spring of seeping flow that issues on the Dinsmore 
ranch, at the west edge of Wolf Creek, has long been protected by a 
concrete curb and used for drinking. Its water is moderately car- 
bonated and sHghtly salty but is pleasing in taste and is much used 
during the summer. On the eastern side of the creek, about 300 yards 
downstream from the main spring, a few seepages issue from a small 
deposit of hme carbonate on the steep bank. On the mountain side, 
about 2^ niiles northward from Dinsmore's, there is a large carbonate 
deposit that is evidently a spring deposit, but little or no water now 
issues near it. 

The rocks on the higher slopes north of Dinsmore's place consist 
mainly of shales and coarser sediments, mth areas of serpentine, but 
near the spring the materials are siliceous, being apparently altered 
shales and sandstones and some chert. 

CARBONATED SPRING NEAR NORTHEAST SIDE OF CLEAR LAKE (LAKE 23). 

In a ravine about half a mile east of Bartlett Landing, which is oji 
the northeast shore of Clear Lake, there is a small carbonated spring- 
that, though known localh', has not been often visited and is of little 
importance. It lies in an area of altered sediments, mainly shales, 
that make up the mountains on the northeast side of the lake and 
are considered to belong to the Knoxville formation of Lower Cre- 
taceous age.^ 

CARBONATED SPRINGS ON CHALK MOUNTAIN (LAKE 25). 

Chalk Mountain hes about 11 miles in a direct Une east of north 
from the town of Lower Lake, and in the bend of Cache Creek, where 
it swings from a westerly to a southerly course. The mountain is 
more properly the end of a ridge and received its name because 
altered lava, which partly composes it, forms white slopes that make 
it a prominent landmark from the north. The lava appears to have 
been altered by solfataric action similar to that which has taken place 
at Sulphur Bank (Lake 38). (See p. 98.) On the northwestern side 
of Chalk Mountain a spring deposit of lime carbonate extends for 

1 See Becker, G. F., Geology of the quicksilver deposits of the Pacific slope: U. S. Geol. Survey Mon. 
13, Sheet III of Atlas, ISSS. 



CAHB0XATK11 SPKIXliS. 197 

about 100 yards along iho mountain side and down the slope to Cache 
Creek, 75 feet below. Water still issues along the upper edge of the 
deposit from a number of seepages and from three pools about afoot 
in diameter and 15 and 75 yards apart. Th<^s(> }aeld a total of per- 
haps 3 galh^ns a minute of water, 67° to 70° in temperature, which 
tastes strongly of hydrogen sulphide, carbon dioxide, and common 
salt. The taste of hydrogen sulphide is the most noticeable and the 
springs are locally known as sulphur springs, but they are here classed 
with the carbonated springs because of the prominent lime carbonate 
deposit that has been formed. Along the side of the mountain, about 
250 yards west of south from the main deposit, another seepage area 
several yards wido is crusted with lime carbonate, but in July, 1910, 
no water was seen. 

ALUM SPRING (LAKE 26). 

Alum Spring seeps from a claylike layer in bedded gravel and 
volcanic ash, beneath a small baiik on the side of a ravine at the 
southwest base of Chalk Mountain, and about one-third of a mile 
south of the carbonated springs just described. The water tastes 
sour and astringent, and considerable efflorescence of alum salts 
forms on the bank and on the slope below it. The flow of the spring 
is small and is probably supphed by surface water, but it appears to 
be continuous. Although it is not a noticeably carbonated spring, it 
is described with the other springs on Chalk Mountain, for in general 
character it appears to resemble them. At the main springs sulphides 
and hydrogen sulphide are apparently in solution in addition to carbon 
dioxide, whereas at Alum Spring acid sulphates and probably free sul- 
phuric acid are formed. None of the springs on the mountain have 
been used, but they are known locally and are occasionally visited 
as points of interest. 

HOUGH SPRINGS (LAKE 13). 

Hough Springs (PI. VI, -4, p. 92) are situated in the canyon of North 
Fork of Cache Creek, on the stage road from Williams to Bartlett 
Springs (Lake 9, p. 200). The property has long been improved as a 
summer resort. In 1910 a hotel and about a dozen cottages, situated 
in a recess at the base of the hill slopes, furnished accommodations 
for 100 people, while camp grounds and a supply store allowed pro- 
vision for many more. 

There are two springs on the property, one being known as the 
Soda and Iron Spring, the other as the Magnesia Spring. The for- 
mer is at the base of steep slopes about 125 yards south of the 
hotel. A basin has been formed at this spring by excavating be- 
neath the base of a considerable deposit of lime carbonate. This 
basin is protected by a cement wall and by a roof, and }aelds a smaU 



198 SPRINGS OF CALIFORNIA. 

flow of moderately carbonated water that is much appreciated for 
drinking. A small pool of only slightly carbonated water that col- 
lects in a basin on the side of the carbonate deposit, above the main 
pool, furnishes another drinking water of less mineralized character. 
The Magnesia Spring is about 75 yards farther to the southeast and 
issues at the base of the mountain slope, beside a small ravine. It is 
also protected by a roof and yields a small flow of carbonated water 
that is noticeably warmer than the main spring and has a different 
taste. A well 20 feet deep beside the store building, which is about 
200 yards north of the springs, is artesian in character, and nearly 
overflows in whiter. It yields water that is considered to be sul- 
phureted but that tastes only mildly carbonated and slightly of 
iron. Another weU 50 feet south of it was bored to a depth of 65 
feet in search of fresh water, but it struck only salty water and was 
abandoned. 

The rocks of this locahty seem to be the crushed and altered sedi- 
ments that are common in the Coast Ranges. Serpentine was not 
observed near the springs, but it may outcrop on the steep, brushy 
slopes above them. 

CARBONATED SPRINGS ON WILEY RANCH (LAKE 12). 

There are several carbonated springs on the Wiley ranch, in the 
canyon of a branch of North Fork of Cache Creek, about 2^ miles 
northwest of Hough Springs. In 1910 they were reached only by a 
steep and rocky trail and were not generally laiown. The springs 
issue in a long glade 100 to 300 yards wide. Tlae water of two or 
three is shghtly sulphureted, but carbon dioxide is the most notice- 
able constituent in the principal ones. The rocks of the locality are 
the usual altered sediments, being mainly siliceous sandstones that 
in some places have a schistose character. 

ALLEN SPRINGS (LAKE 11). 

Allen Springs are situated in the narrow canyon of Allen Creek, on the 
stage road about 4 miles west of Hough Springs (Lake 13, p. 197) . The 
property was early improved as a resort, but high water a number of 
winters ago washed away some of the cottages, and for several years 
the place was closed. In the summer of 1910 it was reopened, how- 
ever, and accommodations for guests were pro^dded by a hotel building 
and several cottages. 

A number of carbonated springs issue along the edge of the creek 
above (west of) the hotel, and strings of bubbles that rise at several 
places in the creek near them show that gas and probably water also 
issues in the stream bed. One spring, whose water was formerly 
bottled, issues from the steep canyon side south of the hotel, across 
the creek, and is piped to a drinking shed. A group of three or four 



CARBONATED SPRINGS. 



199 



principal siiul several minor s[)rings is situated at tiie creek e(lj2;c about 
250 yards northwest of the hotel. One of these, whicli is known as 
the Chalybeate Spring, is suri-ouiuled l)y a cement basin and yields 
perhaps 5 gallons a minute (^f carbonated water, 63° in tem))erature. 
This water is renihn-ed turbid by iron in suspension. Tlie following 
analysis, believed to represent water from this sj^ring, indicates that 
it is secondarv alkaline in character: 



Analysis of water from Chalybeate S pring , Allen Springs, Lake County, Cal. 
[Analyst and authority, AVinslow .Vnderson (1888). Constitueut.s ai'e iu parts per million.] 



Temperature 

Properties of reaction: 
Primary salinity 

Secondary salinity. . . 

Tertiary salinity 

Primary alkalinity. . . 
Secondary alkalinity , 
Tertiary alkalinity.. 



W ('. (.iS" F.) 

S'.i 


4 

57 
73 



Constituents. 



By 
weight. 



Reacting 
values. 



Sodium (Na) 

Potassium ( K) . . . 

Calcium (Ca) 

Magnesium (Mg). 
Iron ( 



(Fe). 



Sulphate (SO4)-.. 

Chloride (Cl) 

Carbonate (CO3). 
Phosphate (POO - 
Silica (Si02)o 



Carbon dioxide (CO2) . 



180 
22 
89 
81 
7.5 
9.1 
263 
359 
5.7 



1,016.3 



306 



4.44 

6.64 

27 

!i9 

7.42 

11.95 

.18 



13.93 



a Not reported. 

About 20 3^ards eastward, across the creek from the Chalybeate 
Sprmg, there is a sulphur spring wliich yields about 1^ gallons a 
minute of slightly carbonated and distinctly sulphureted water 
which has a temperature of 56°. Another spring, known as the 
Sureshot, issues at the creek edge 150 yards upstream. It is the 
westernmost one that has been improved and is locally considered 
to be the most strongly mineralized. Like the Chalybeate Spring, 
it is turbid, but it yields only a shght flow. Half a mile west of the 
buildings at Allen Springs there is a small but vigorously bubbling 
and pleasantly carbonated spring at the roadside. A few small 
lime-carbonate deposits on the liillside show wheie carbonated water 
also formerly issued and perhaps still seeps out. 

All of these springs emerge from sihceous altered sediments that 
are cherty in character on the slope south of Sureshot Spring but 
have a schistose appearance along the creek bed near the Chalybeate 
and Sulphur springs. A small amount of serpentine is exposed a 
few hundred yards east of the hotel, but none was seen near the 
springs. 



200 



SPRINGS OF CALIFOENIA. 



BAB.TLETT SPRINGS (LAKE 9). 

For several years Bartlett Springs (PI. XII, 0) have formed a 
summer resort in Lake County. The property is situated on the 
north side of a branch of North Fork of Cache Creek, and mainly 
on the slopes some distance above the stream. A number of small 
cottages were earl}^ built near the springs and othere have been added 
from time to time. A commodious hotel, stores, pleasure buildings, 
and a large bottlhig house have aided in making a considerable 
settlement at the place. 

The Main Spring is situated in the northern part of the grounds, 
at the base of steep slopes. It has been improved with a tin-lined 
cement basin elevated above a cement floor. This basin is used as a 
drmking fountain, and pipes lead from it to a small fountain at the 
hotel and to the bottling house. The water is cool (56°), is mildly 
carbonated, and is shown by the analysis to be secondary alkaUne 
in character. 

Analyses of water from Bartlett Springs, Lake County, Cal. 
[Constituents are in parts per million.] 



Temperature 

Properties of reaction: 

Primary salinity 

Secondary salinity . . . 

Tertiary salinitj^ 

Primary alkalinity. . . 
Secondary alkalinity . 
Tertiary alkalinity . . 



3 

2 


95 
620 



12° C. (54° F.) 

2 


1 

97 
695 



(7) 



Constituents. 



By 
weight. 



Reacting 
values. 



By 

weight. 



Reacting 
values. 



By 

weight. 



Reacting 
values. 



Sodium (Na) 

Potassium (K) 

Lithium (Li) 

Ammonium (NHj). 

Barium (Ba) 

Calcium (Ca) 

Magnesium (Mg). . . 

Iron (Fe) 

Aluminum (Al) 

Sulphate (SO4) 

Chloride (01) 

Carbonate (CO3)... 
Metaborate (BO2).. 
Phosphate (PO4)... 
Smca(Si02) 



Carbon dioxide (CO2) . 



9.4 

2.3 

Trace. 



.41 

.06 

Trace. 



Trace. 
206 
44 
4.2 



Trace. 

10.28 

3.61 

.15 



8.3 

2.7 

Trace. 

Trace. 

.7 

213 

33 

Trace. 



.36 

.07 

Trace. 

Trace. 

.01 

10.63 

2.69 

Trace. 



30 

5.7 

407 

Trace. 

5.4 

64 



.62 

.16 

13.56 

Trace. 

.17 

2.12 



7.7 
5.3 
399 
Trace. 
5.1 
59 



.16 

.15 

13.29 

Trace. 

.16 

1.97 



6.1 
11 
1,323 



50 



778.0 



733.8 



2,010.1 



2,060 



4.24 
39.32 



.13 

.31 

44.09 



1. Mainspring. Analyst and authority, Winslow Anderson (1888). 

2. Main Spring. Analyst, G. E. Colby (1880 ?). Authority, Winslow Anderson. 

3. Soda-magnesia Spring. Analyst, Southern Pacific Co. (?) (1900). Authority, advertising matter. 



Aperient Spring is on the hillside, about 200 yards by zigzag trail, 
northeast of the Main Spring. It issues in a small springhouse, 
and yields perhaps 2 gallons a minute of moderately carbonated water 



CARBONATED SPRINGS. 201 

61° in temperature, which deposits considerable iron. Its water htus 
been used for drinking and has also been piped to aswimniinj^; plunge. 

The Soda-magnesia Spring is about 100 yards southeast of Aperient 
Sprmg at the base of a steep slope. It yields perhaps 3 gallons a 
minute of cool, mildly carbonated water that is piped to large storage 
tanks near by and thence to the grounds. like the water of Aperient 
Spring, it deposits considerable iron along its overflow channel. 

The analyses on page 200 show that Soda-magnesia Spring con- 
tains a considerably larger propoition of magnesium than the water 
of the Main Spring and is essentially secondary alkaline in character. 

The Gas Spring is about three-fourths of a mile by trail northeast 
of the Main Spring and is across a divide on slopes that drain to 
North Fork of Cache Creek. The spring consists of a shallow pool 1 
to 3 feet wide and about 10 feet long, partly beneath a small })ank on 
the canyon side. There is only a seepmg overflow in summer, but 
the pool is kept in vigorous ebullition by large bubbles of carbon 
dioxide that continually escape. The amount of this gas is so great 
that it extinguished a lighted newspaper held 8 inches above the 
surface of the pool. 

The Main Spring at Bartlett Sprmgs apparently issues from altered 
sandstone, but serpentine is exposed a few yards to the north. 
Aperient Sprmg also issues from altered sediments, but serpentine 
outcrops a few yards north and west of it. The steep slope back of 
the Soda-magnesia Sprmg is formed by a ledge of hard, altered sand- 
stone. Shale forms the slopes near the Gas Spring, but there is a 
small exposure of decayed serpentine a few yards east of it. All of 
this region appears to be composed of the altered sediments and 
associated serpentine that are a characteristic rock formation in 
Lake County. 

HOPPmS SPRINGS (LAKE 10). 

The property of Hoppins Sprmgs, which joins the eastern boundary 
of that of Bartlett Springs, has been improved to some extent as a 
resort by the erection of several cottages for light housekeeping. 

Two small springs that issue on the property, about 100 and 150 
yards east of the Bartlett Soda-magnesia Spring, are known respec- 
tively as the Magnesia Spring and the Iron Spring. Each forms a 
drinking pool that has been protected by a board cover and contains 
cool, carbonated water. That of the Iron Spring is the more strongly 
carbonated, and that of the Magnesia Spring has a more pronounced 
taste of iron or magnesia. 

Serpentine is exposed at the roadside a short distance south of the 
springs, but like Bartlett Springs the mineral water apparently 
issues from altered sandstone. 



202 SPRINGS OF CALIFORNIA. 

NEWMAN SPRINGS (LAKE 8). 

Newman Springs are about 1^ miles north of west from Bartlett 
Springs (Lake 9, p. 200), and issue along the channel of Soap Creek; 
hence they are sometimes referred to as the Soap Creek Springs. The 
sprmg farthest downstream — which is the principal one — emerges at 
the creek side at the base of a prominent ledge of serpentine that 
forms the eastern border of a belt of this rock and the contact zone 
between it and crumpled shales and siliceous sediments that continue 
eastward. The sprmg yields about 15 gallons a minute of mildly 
carbonated water 86° m temperature, that is turbid with iron. The 
water is conducted across the creek in a trough to a small plunge bath- 
house. A spring in the creek bed about 75 yards above (southwest of) 
the main spring, forms the Borax Pool, which contains warm, turbid 
water that is considered to be of exceptional value for bathing. The 
serpentine belt continues for about 100 yards upstream (westward) 
from it and is then succeeded by schistose rock, from which seepages 
and slight flows of warm carbonated water issue in at least seven places 
along a distance of about 275 3^ards or to a point about a quarter of a 
mile above the main spring. Temperatures of 72° to 92° were 
noted in these small springs, and the locality is therefore indicated 
in Plate III (in pocket) as containing thermal carbonated springs. 
The position of the springs with respect to the serpentine dike is sug- 
gestive in considering their origin, for this dike may not only afford 
an upward passage of escape for heated water but may possibly also 
be the direct cause of its abnormal temperature. 

HAZEL SPRINGS (LAKE 7). 

About 8 miles northeast of Upper Lake, at Hazel Springs (formerly 
known as Dennison Springs), two small carbonated springs issue 
about 20 yards apart. The property has been used at times as a 
summer camping resort, but during July, 1910, it was closed to the 
public 

ROYAL SPRING (LAKE 6). 

Royal Spring is about 7 miles west of north from Bartlett Springs 
(Lake 9, p. 200), and 2 miles by a slightly used road running north from 
the dairy ranch in Twin Valley. The spring emerges on the side of a 
ravine that is tributary to North Fork of Cache Creek. It has been 
protected by a cement basin in which the water rises cleai', but it 
deposits some iron along its overflow channel. It is cool, moderately 
carbonated, and tastes distinctly of iron or magnesia. In former 
years, when the property was occupied, the spring was better known, 
but it has been used for several summers as a private camping ground 
only. 



CARBONATED SPKINyS. 203 

The position of the spring is significaiil, for it is at the western 
horder of a heh of serpentine that extends in a northerly direction 
through the usual altered sediments. Although tho examination of 
the region was not sufiiciently detailed to determine the positions of 
the springs with respect to the serptnitine areas, it is thought that the 
occurrence of mineralized waters in the northern Coast Ranges is 
closely related to the serpentme areas. Tlie relation seems to be 
especially well shown along the eastern side of Lake and western sid(^ 
of Colusa counties, where tliere is a wide zone of serpentme with 
minor, approximately parallel zones that trend in a general dhection 
west of north. The hot springs of Sulphur Creek (Colusa 9 to 12, pp. 
99-104) are in a serpentine area or near its western border; OilSprmg 
(Colusa 8, p. 194) is m a northern extension of apparently the same 
zone or dike; Complexion Sprmg (Lake 14, p. 297) is m serpentine; 
Bartlett Springs and Iloppins Sprmgs (Lake 9 and 10, pp. 200-201) 
apparently issue at the borders of narrow serpentme dikes; Royal 
Spring (Lake 6) is at the west edge of a serpentme exposm'e whose 
com"se can be easily traced along the hillsides to the nortli and to the 
south; and Crabtree Sprmgs (Lake 5, p. 106) are in siliceous rock that 
is closely associated with serpentine. 

PARAMORE SPRESTG (LAKE 4). 

Pai'amore Spring is situated on a branch of Rices Fork of Eel River, 
about 4 miles in a dhect line northwest of Crabtree Springs (Lake 5, 
p. 106). The spring is in a deep, brushy ravine and is not easily 
accessible, but the place has been visited occasionally^ by campers. 
It yields cool, strongly carbonated water, but it issues at the creek 
edge and is hence available only during periods of low water. 

CARBONATED SPRING NEAR RANGER CAMP (LAKE 3). 

A small carbonated spring near the ridge west of Paramore Sprmg 
has been used in recent years by the Government forest rangers, who 
have estabUshed a camp near by. Like several other springs in the 
region, it yields a small amount of cool carbonated water that is 
appreciated for drinking. 

CARBONATED SPRING ON BEAR CREEK (LAKE 2). 

About 1| miles above tlie moutli of Bear Creek and near the stream 
channel, there is a carbonated sprmg that is known to hunters in the 
region. It has not been improved, however, and is not easily found. 
There are probably other similar springs in the rugged parts of north- 
ern Lake County whose positions are known chiefly to residents of 
the region. 



204 



SPRINGS OF CALIFORNIA. 



MORTON SODA SPRING (LAKE 1). 

Morton Soda Spring is situated near the moutli of Soda Creek^ 
wliicli joins South Fork of Eel River about 2 miles south of west of 
HuUville. The sprmg yields a small flow of cool carbonated water 
that is very pleasant for drinking, but it has been known and used 
only locally. 

COOKS SPRINGS (COLUSA 5). 

Cooks Sprmgs (PL XII, A, p. 200) have been a well-known summer 
resort for a number of years, and the water has long been marketed 
for table use. In 1910 accommodations were provided for 150 people 
by a well-appointed hotel and a number of cottages. The place is 
situated in the lower portion of the Coast Ranges west of Sacramento 
Valley, and the grounds extend along two ravines that unite near 
the hotel to form a tributary of Stony Creek. 

There are three principal springs on the property, the main one 
being about 40 yards southeast of the hotel and beneath the roof that 
covers a bowling alley. A cemented, covered reservoir has been 
constructed at the spring. Over it a small hand pump supphes water 
for drinking, and a pipe leads from the reservoir to a bottlmg house 
about 125 yards northward, down the ravine. The spring yields 
perhaps 2 gallons a minute of moderately carbonated water, 64° in 
temperature, which tastes shghtly saline. 

The following analysis shows the water to be secondary alkaline in 
character with notable primary salinity and alkalinity. The large 
proportion of magnesia is also noteworthy. 



Analysis of ivater from Main Spring, Cooks Springs, Colusa County, Cal. 
[Analyst, R. E. Swain (1900). Authority, advertising matter. Constituents are in parts per million.] 



Properties of reaction: 

Primary salinity 

Secondary salinity 

Tertiary salinity 

Primary alkalinity 

Secondary alkalinity 

Tertiary alkalinity 

Constituents 

Sodium (Na) 

Calcium (Ca) 

Magnesium (Mg) 

Iron ( Fe) 

Aluminum ( Al) 

Sulphate (SOj) 

Chloride (01) 

Carbonate (CO3) 

SUica (Si02) 

Carbon dioxide (CO2) 



14 


21 
65 
46 



By 

weight. 



Reacting 
values. 



624 
26 
614 
5.6 
1.9 
6.0 
390 
2,015 



27.14 

1.29 

49.65 

.20 

.21 

.12 

11.00 

67.16 

2.65 



3, 762. 5 



731 



33.22 



CARBONATKl) SPUIXCS. 205 

Iron Spring- issues ou the hillside about oOO yards south of the 
Main Spring ami (35 yards northeast of the dancing hall. A cemented 
basin at this sj)riug, at the base of a small bank ])eneath a ])rotecting 
roof, yields perhaps a quarter of a gallon a minute of water that tastes 
similar to that from the Main Spring but noticeably stains its run- 
off channel with iron. About 700 yards south of the dancing hall, 
at the creek side, there is an efl'ervescing carbonated s])ring that is 
called the Sulphur Spring, as its water has a slight odor of hydrogen 
sulphide, but it is primarily a carl)onate(l spring. A concrete wall 
along the creek protects the spring and forms a reservoir in which 
its flow of about 5 gallons a minute collects. Thence a pipe extends 
down the ravine to tlie swimming pool near the hotel. It is said 
that attempts to bottle the water have been unsuccessful because its 
large content of carbon dioxide breaks the bottles. 

Among minor springs on the property are two or three vents in 
the creek bed a few yards above the Sulphur Spring, from which 
the water bubbles, and two noncarbonated springs of seeping flow 
at the creek side, behind the store and hotel annex ])uilding, which 
adjoins the main hotel. Small noncarbonated springs that are used 
for drinking also issue from the bank back of the bottling house and 
at the roadside about half a mile below the resort grounds. 

Sedimentary rocks form the hills westward from Sacramento Val- 
ley to within about 1^ miles of Cooks Springs. Serpentine thence 
extends westward and forms the slopes at and near the resort grounds. 
In some places this rock is altered so that it reseml)les siliceous 
material, but massive serpentine is exposed in the road bank 40 
yards northeast of the hotel. Pyroxene rock that exhil)its concentric 
w^eathering unusually well is shown in a roadside cut 100 yards west 
of the hotel. A few hundred yards farther west, up the ravine, the 
serpentine has been much broken and the fragments have been 
cemented by calcite into a breccia. Several tunnels have been 
driven into this material in search of copper ore. 

The Main Spring and the Iron Spring issvie from serpentine, but 
the Sulphur Spring, which is the largest and most strongly carbonated, 
issues from material that appears to be dark, altered sandstone con- 
taining veinlets of calcite. The exposure of this rock may indicate 
that it is present beneath the surface at the other springs, and the 
calcite in it may yield the carbon dioxide of the springs. Carbon 
dioxide that is given off by magnesite and other carl)onates formed 
from the serpentine may, however, as plausibh" account for the carbon 
dioxide. 

FOUTS SPRINGS (COLTJSA 3). 

Fouts Springs have been resorted to during the summer for 40 
years or more. In 1905 the propertv changed o^\^lership and since 
then it has been greatly improved. The buildings are located on a 



206 SPRINGS OF CALIFORNIA. 

gentle slope at the eastern base of a brushy mountain and are about 
10 miles by road westward from Stonyford, across a mountain 
divide. In 1910 about 30 cottages, a dozen tents and a building 
containing an office and a dining hall, furnished accommodations 
for 150 guests. 

There are four principal springs on the property. Champagne 
Spring, which is the one most used for drinking, rises in a pool beneath 
the floor of a spring house near a small creek and about 175 yards 
southwest of the dining hall. It yields a small flow of pleasantly 
carbonated water that is much appreciated for drinking. The 
analysis shows it to be a moderately mineralized water, secondary 
alkaline in character, markedly dift'erent from the waters of the other 
two springs that have been analyzed. In the creek bed, about 20 
yards south of the spring, carbonated water issues with much bub- 
bling, but in 1910 these springs had not been improved nor used. 

The three other springs, or groups of springs, are in a ravine one- 
half to three-fourths mile northwest of the resort grounds. Redeye 
Spring receives its name from the rusty-red stain of iron along its 
overflow channel. The water issues from seams in the rock on the 
north bank of the creek, where two small basins yield about one-half 
gallon and 5 gallons a minute of carbonated saline water that has a 
temperature of 75°. This water was formerly bottled and marketed 
and is still used for drinking, but, as is shown by the analysis, it 
is too salty to be pleasant to the taste. Many bubbles that rise in 
the creek near Redeye Spring show that gas and probably also carbon- 
ated water issue from other seams m the rock at this place. 

The Bath or New Life Sprmg is about 175 yards westward, upstream, 
from Redeye Spring and on the same side of the creek. The main 
flow comes from a pool 2 feet in diameter, which yields about 8 
gallons a minute, and a small pool 3 yards away yields perhaps 
one-half gallon a minute more. The water has a temperature of 
75° and tastes moderately carbonated and salty, like that of Redeye 
Spring, which analysis shows it to closely resemble, both being 
primary saline and secondary alkaline in character, but it has built 
up a terrace of gravel and lime carbonate about 5 yards wide and 20 
yards long at the side of the creek. The water is conducted in 
a trough eastward to a bathhouse a short distance below Redeye 
Spring and heated for bathing. It deposits much calcium carbonate 
in the trough, though the following analyses show that it contains 
the least calcium of the three sj)ring waters. Noteworthy features 
of the waters shown by the analyses are the amounts of iodine, 
ammonium, and nitrate. 



CARBONATED SPRINflS. 



207 



Analyses of water froiii Fonts iiprings, Colusa i'ounty, Cal. 

(Amilvst, U. S. Bureau of Chemistry (1906?). Authority, owner of springs. Constituents are in parts 

per million.) 



Properties of reaction: 

I'rimary salinity 

Secondary salinity 

Tertiary salinity 

Primary alkalinity 

Secondary alkalinity . . 
Tertiary alkalinity 

Constituents 

Sodium (Na) 

Potassium (K) 

Ammonium (NHi) 

Calcium (Ca) 

Ma^iesium (Mg) 

Iron (Fe) 

Sulphate (SO4) 

Nitrate (NO3) 

Chloride(Cl) 

Bromide (Br) 

Iodide (I) 

Carbonate (CO-,) 

Metaborate (BO2) 

Nitrite (NO2) 

Phosphate (PO4) 

Silica (Si02) 

Carbon dioxide (CO2) 



Champagne 
Spring. 



(?) 



By 

weight. 



Reacting 
values. 



liath or New Life 
Spring. 



(?) 



By 
weight. 



Reacting 
values. 



He<leye Spring. 



(?) 



By 
weight. 



Reacting 
values. 



5.8 
Trace. 
139 
118 
1.4 
5.5 
15 
40 


467 



66 



2.97 

.15 

Trace. 

6.93 

9.67 
.05 
.12 
.24 

1.13 
.00 
.00 
15.58 
.00 
.00 
.00 

2.19 



4,859 

34 

38 

132 

204 

2.4 

13 

44 

5. 591 

Trace. 

23 

2. 188 

Trace. 





113 



211.26 

.86 

2.12 

6.59 

16.74 

.09 

27 

In 

1.57. 67 

Trace. 

.18 

72. 95 

Trace. 

.00 

.00 

3. 75 



4.879 

62 

8.6 

162 

308 

3.5 



5.221 
Trace. 

41 

2.780 

Trace. 





116 



212. 13 

I..59 

.48 

8.11 

25. 38 

.13 

.11 

1.43 

147. 24 

Trace. 

.32 

92.67 

Trace. 

.00 

.00 

3.85 



925.7 



13,241.4 



13.674.3 



Present. 



Present. 



Present. 



Present. 



Present. 



Present. 



Sulphur Spring, which yiolds about 2 gallons a minute of pleasant- 
tasting, mildly sulphureted water, 60° in temperature, issues on the 
south side of the creek beneath an irrigating flume and 225 yards 
west of the Bath Sprhig. Like that of Redeye Spring, its water 
is used to some extent for drinking, but the spring is too far from the 
main grounds to be fully appreciated. 

The carbonated springs — the Champagne, Redeye, and Bath 
springs — issue from serpentine, which at Redeye and Bath springs 
is weathered to a light-colored but hard material. The bowlders in 
the creek bed consist of altered sandstone veined with quartz and 
calcite, and the Sulphur Spring issues from a steep slope of crushed 
rock of this character. It is worthy of mention here that two other 
sulphur sprmgs in this locality, one (Colusa 2, p. 267) southwest, and 
the other (Colusa 1, p. 267) west of Fonts Sprmgs, also issue from the 
altered sediments. As elsewhere in the Coast Ranges, the serpentine 
is probably intrusive in the altered sediments, and the carbonated 
springs are apparently closely related to the presence of the serpen- 
tine. The salty character of the water of Redeye Spring and Bath 
Spring seems to be accounted for by the presence of the altered sedi- 
ments. 



208 SPEIWGS OF CALIFOENIA. 

FERNDALE SPRINGS (CONTRA COSTA 1). 

• Ferndale Springs are in Vaca Canyon, about 6 miles (by road) 
south of Martinez. Two springs of small flow issue from a steep bank 
on tlie southern side of the canyon, about 50 feet above the creek, and 
were formerly piped across it to bottling works on the opposite side 
of the canyon. In 1908, however, bottling had been discontinued 
for a year or more. A small tminel has been excavated at the prin- 
cipal sprmg, which jdelds a flow of perhaps 1^ gallons a minute of 
noticeabty carbonated water. The rocks consist of shale and soft 
fine-grained buff sandstone, the spring issumg from a bank of thick- 
bedded sandstone. 

ALUM ROCK PARK SPRINGS (SANTA CLARA 3). 

Alum Rock Park is in Alum Rock Canyon, about 7 miles northeast 
of San Jose. The property was purchased from the Spanish Govern- 
ment by the Pueblo de San Jose and still belongs to the city, being 
conducted as a recreation park. It received its name from an alum- 
coated bowlder that lies in the grounds. The improved part of the 
park extends for about 600 yards along the narrow canyon and has 
been partly laid out with walks and garden plots. Tub baths and a 
swimming plunge have been constructed, and a cafe, Japanese tea 
garden, candy booth, and a few other concessions have been granted 
in order to help defray the expense of mamtenance. The place is 
easily reached by electric car from San Jose. 

At least 16 nimeral sprmgs issue along the park at the bases of the 
canyon sides, their positions being shown on the sketch map (fig. 4). 
The sprmgs differ notably in the chemical characteristics of their 
waters. AH are distinctly sulphureted, four are moderately car- 
bonated, and one deposits considerable amounts of iron. A seven- 
teenth sprmg, which is noticeably salme and is known as the Salt- 
Condiment Sprmg, issues in a little ravme 600 yards west of the 
lower end of the park grounds. It is piped to a drinking basin at the 
roadside a few yards away. 

Thu'teen of the sprmgs, including the Salt-Condiment Spring, have 
been improved by cement or rock-mas omy basms to form drmkmg 
pools, and water from at least two of them is also piped to the baths. 
The other four — the one that deposits hon, a sulphur spring, and two 
carbonated springs that deposit lime carbonate — issue in tunnels 
that have been run into the canyon sides a few feet above the level 
of the other springs. They have been used in part to supply water 
for the baths. 

Two drinkmg sprmgs that issue from pipes side by side near the 
upper end of the park are worthy of special mention. One of them 
yields water that is milky from suspended sulphur, and the water 



CARBONATED SPRINGS. 



209 




35657°— W8P 338—15- 



-14 



210 SPEINGS OF CALIFORNIA. 

from the other is ahnost black from iron sulphide. The latteir effect 
has, however, possibly been artificially produced by bringing together 
the flows of an iron and a sulphur spring. 

As most of the springs are sulphureted, the locahty might be prop- 
erly described with the sulphur springs, but the carbonated springs 
are most used for drinking and are probably as characteristic of the 
place. 

The following analyses show the chemical character of the principal 
springs. The Salt-Condiment Spring is characterized chiefly by pri- 
mary salinity, but secondary salinity is notable; the Soda Spring is 
primary alkaline in character; and the other springs, though differing 
widely in concentration and exhibiting many minor differences in 
composition, are all of mixed type — primary alkahnity, secondary 
alkalinity, and primary salinity all being prominent. 

All of the springs are of small flow. Only four of them discharge 
more than 1 gallon a minute, and each of these four yields less than 
5 gallons a minute. The temperatures are above the normal, ranging 
from 69° to 87°. 

The rocks at Alum Rock Park consist of beds of shale and sand- 
stone of Tertiary age that have been highly tilted and folded. These 
sediments are probably the direct source of the main constituents 
in the spring waters. 



CARBONATED SPRINGS. 



211 





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212 SPRINGS OF CALIFORNIA. 

Chemical reactions that take place after the solution of the min- 
erals may account in part for the abnormal temperatures of the 
springs; the intense movement that has tilted the beds at steep 
angles may also have produced a high thermal gradient, and thus 
partly account for them. 

GRANT SPRING (SANTA CJ,ARA 2). 

About 5 miles above Alum Rock Park there is a small carbonated 
spring which is known as Grant Spring. Its water has been bottled 
and placed on the local market for table use. 

The rocks at this locality appear to be the same as those lower down 
the canyon, and the spring seems otherwise to be similar in occur- 
rence to the springs in Alum Rock Park. 

CONGRESS SPRINGS (SANTA CLARA 5). 

Congress Springs, which were formerly known as Pacific Congress 
Springs, are in a canyon near the edge of Santa Clara Valley, 12 
miles southwest of San Jose. They were improved for many years as 
a resort, and the water formerly was in considerable demand for table 
use, but in 1903 or 1904 the hotel burned, and since that time the 
property has not been so well kept up. 

Two small carbonated springs rise at the upper end of the grounds, 
on the north bank of Campbell Creek. A spring house has been 
erected over one of them, and a portion of its flow rises in a cemented 
brick drinking basin. The other spring is 30 yards farther upstream. 
A small house that inclosed a gas-collecting tank stood over it in 
1908. Its gas (carbon dioxide) and water were formerly piped to 
bottling works a short distance below the lower spring. The analysis 
(p. 213) probably represents water from the upper spring and indicates 
that it is a primary alkaline and saline water containing a large pro- 
portion of iron and aluminum. 

A considerable deposit of lime carbonate appears in the bed of 
Campbell Creek 200 or 300 yards below the springs. The position 
and character of this deposit suggests that it was formed at a time 
when carbonated water emerged at or near that place. 

The springs issue in an area of dark-gray sandstone that belongs 
to the Franciscan formation. This material is cut by dikes of dark- 
gray diabase, and it is thought that a small dike of this rock crosses 
Campbell Creek a few yards above the upper spring. If this is true, the 
dike rock may have some influence on the rise of carbonated water 
at this place. 

AZTJLE MINERAL SPRING (SANTA CLARA 4). 

Azule Mineral Spring is situated in a ravine a mile northward 
across a divide from Congress Springs. It was first known as Mills 
Seltzer Spring, but the name was early changed to Azule, from the 



CARBONATED SPRINGS. 



213 



blue appoaranco of the mountains to the southwest. The water was 
formerly bottled for table use, but it has not been on the market 
since about 1890. The property has, however, been improved as a 
picnic resort. 

The spring rises in a small concrete house, from a crevice in dark- 
colored sandstone. Water also issues beside the spring house, ap- 
parently from the same crevice as that within the house, and the com- 
bined flow of the two streams is perliaps a quarter of a gallon a minute. 
The water is strongly carbonated and also tastes slightly of hydrogen 
sulphide. A very small deposit of Epsom salt was noticed beside 
the spring, and the channel is iron stained for a few yards below it. 
There are small deposits of lime carbonate farther downstream. 

Although the spring issues from sandstone, serpentine that ap- 
pears to form a dike not much more than 10 yards thick is exposed 
on the slope immediately above it. This dike may determine the 
position of the spring at this point, and the considerable amount of 
magnesia in the water that is shoAvn by the following analyses, 
tabulated with one from Congress Springs, is probably explained by 
the presence of the serpentine. The water may be classed as sec- 
ondary alkaline and primary saline, but the unusually large content 
of magnesium is noteworthy. 

Analyses of water from Azule Mineral Spring and Congress Springs, Santa Clara 

County, Cal. 

[Constituents are in parts per million.] 



Temperature 

Properties of reaction; 

Primary salinity 

Secondary salinity . . . 

Tertiary salinity 

Primary allcalinity . . 

Secondary alkalinity. 

Tertiary alkalinity . . . 



16° C. (00° F.) 

39 



13 

48 
140 



42 


11 
47 
136 



10° C. (50° F.) 

43 


36 
21 
42 



Constituents. 



By 
weight. 



Reacting 
values. 



By 
weight. 



Reacting 
values. 



By 

weight. 



Reacting 
values. 



Sodium (Na) 

Potassium (K)... 

Calcium (Ca) 

Magnesium (Mg). 

Iron (Fe) 

Aluminum (Al).. 
Sulphate (SOi)... 

Chloride (01) 

Carbonate (CO3) . 
Silica(Si02) 



Carbon dioxide (CO2) . 



972 
126 
69 
462 



42.25 
3.21 
3.44 

38.02 



990 
117 
62 
462 



43.03 
2.86 
3.08 

37.99 



1,212 

1,582 

55 



34.17 

52.75 

1.82 



1.280 
1,526 



36.10 
50.86 



1,746 

20 

181 

144 

115 

41 

378 

1,201 

1,790 

68 



75.90 

.51 

9.05 

11.87 
4.10 
4.52 
7.87 

a3.89 

59.67 
2.26 



4,478 



4, 437 



5,684 



2,606 



756 



1. Azule Mineral Spring. Analyst and authority, Winslow Anderson (1888). 

2. Azule Mineral Spring (bottled water). Analyst, James Howden. Authority, U. S. Geol. Survey 
Bull. 32. 

3. Upper spring, Congress Springs. Analyst and authority, Winslow Anderson (1888). 



214 SPEINGS OF CALIFORNIA. 

Congress and Azule springs form a rather isolated group of car- 
bonated springs, for springs of this character are not common in this 
part of the Coast Kanges. There was formerly a carbonated spring 
about 200 yards east of the reduction works at the New Almaden 
quicksilver mine, 15 miles southward from San Jose, but the crevice 
or other source from which it received its carbon dioxide was cut 
through by mining operations, and the spring has been dry for many 
years. During the seventies its water was bottled and marketed as 
New Almaden Vichy Water, and in later years it was also pumped 
for bottling. An approximate analysis^ showed that it contained 
considerable sodium, calcium, bicarbonate, sulphate, and free carbon 
dioxide. 

MADBONE SPRING (SANTA CLARA 8). 

Madrone Spring is situated on a tributary to Coyote Creek, 14 
miles east of Madrone station. There were several cottages and a 
small hotel on the property as early as 1880, and in 1891 a larger 
hotel was erected. In 1908 the place was conducted mainly as a 
hunters' resort, with accommodations for about 50 people. A trail 
leads southeastward over the hills 6 miles to Gilroy Hot Springs. 

The spring issues at the southern edge of the stream channel, 
beside a dancing paviUon that has been built over the creek. When 
visited the water issued in a cemented basin that had no appreciable 
overflow and was lifted to the level of the pavihon by a hand pump. 
In 1892, and for a few years following, the water was taken in barrels 
to San Jose and bottled. The analysis tabulated on page 215 shows 
that the water is essentially primary and secondary alkaline. 

On the slopes south of the hotel are two unused seepages that are 
called ''arsenic" and "iron" springs but do not appear to be notably 
mineralized. A quarter of a mile westward, up the creek, a faintly 
sulphureted spring that yields about one-half gallon a minute issues 
at the southern edge of the stream; it has been protected by a box 
curbing that forms a small drinking basin. 

The carbonated spring rises from dark-colored shale which is ex- 
posed along the creek for 50 or 75 yards above and below it. A Httle 
farther downstream, thick-bedded sandstone is exposed, and eastward 
from it, the sediments are siliceous and cherty. The series dips 
nearly vertically northeast and strikes northwestward across the 
creek. 

COES SPRING (SANTA CLARA 7). 

In a ravine about IJ miles west of Madrone Spring, on the Coe 
ranch, carbonated water rises in a stream channel, amid bowlders of 
sandstone, and in 1908 a pipe conducted it from a small basin in the 

1 California State Mineralogist Sixth Kept., p. 73, 1886. 



CARBONATED SPRINGS. 



215 



stream bed to a cattle-watering trough a few yards below. A small 
amount of iron-stained, lime-cemcntcd gravel has been formed along 
the creek below the spring. The sandstone near by is much veined 
by secondary material, and some serpentine float was noticed. The 
formation, however, seems to be of sandstone and shales similar to 
those at Madrone Spring, but these materials dip less steeply toward 
the northeast than they do at the latter place. The following analysis, 
tabulated with one from Madrone Spring, shows that the water of the 
Goes Spring is the less strongly minerahzed and that it is secondary 
alkaline in character, magnesium being present. 

Analyses of water from Madrone and Goes springs, Santa Clara County, Col. 
[Authority, 13th Cal. Constituents are in parts per million.] 



Properties of reaction: 

Primary salinity 

Secondary salinity. . . 

Tertiary salinity 

Primary alkalinity. . . 
Secondary alkalinity. 
Tertiary alkalinity . . . 



Constituents. 



By 
weight. 



Reacting 
values. 



weight. 



Reacting 
values. 



Sodium (Na) 

Potassium (K) 

Lithium (Li) 

Barium (Ba) 

Strontium (Sr) 

Calcium (Ca) 

Magnesium (Mg). . 

Iron(Fe) 

Aluminum (Al)... 
Manganese ( Mn) . . 
Sulphate (SOi)... 

Chloride (CI) 

Carbonate (CO3) . . 
Metaborate (BO2). 
Phosphate (PO4).. 
Silica (Si02) 



217 
7.4 
Trace. 
1.2 
Trace. 
380 
37 
4.7 



9.45 

.19 

Trace. 

.02 

Trace. 

18.94 

3.04 

.17 



56 



2.45 



182 

21 

Trace. 



4.47 

14.94 

.74 

Trace. 



.03 



14 

940 

Trace. 

3.2 

108 



.40 

31.34 

Trace. 

.10 

3.60 



27 
6.4 
649 



.57 

.18 

21.63 



7.0 
97 



.22 
3.21 



1,713.3 



1,135.4 



Carbon dioxide (CO2). 



Present. Present 



Present. 



Present. 



1. Madrone Spring. Analyst, G. E. Colby. 



2. Coes Spring. Analyst, M. E. Jafla. 



BANES SODA SPRINGS (MONTEREY 7). 

Banes Soda Springs are situated on the coast about 6 miles south- 
west of the Cruikshank mines, in southern Monterey County. Car- 
bonated water issues for a considerable distance along a bluff that 
here borders the ocean and has deposited notable amounts of lime 
carbonate. At the main spring a terrace several feet in height has 
been built by the iron-stained material that has been deposited 
from solution. 

The water apparently derives its contents of calcium and of 
carbon dioxide from limestone- masses that are associated with the 
other altered sediments along this portion of the coast. 



216 SPEINGS OF CALIFORNIA. 

HELMS SODA SPRINGS (MONTEREY 8). 

Helms Soda Springs are about 3 miles east of Banes Soda Springs. 
Their water is strongly carbonated, but the flow is slight, and they 
have not formed a notable deposit such as is formed at the springs 
farther west. 

GARRETSON SODA SPRINGS (SISKIYOU 1). 

Near the northeastern border of the State there are a few car- 
bonated springs along the branches of Beaver Creek, in a region 
that is composed mainly of altered rocks. Of these, the best known 
are Garretson Soda Springs, which lie on the northern side of the 
canyon of West Fork of Beaver Creek, about 500 feet above the 
stream. The place has been a camping resort for a number of 
years, and as many as 225 people have been there at one time. In 
1909, however, it was reached by 9 miles of trail from the terminus 
of the wagon road, and few camping accommodations were provided. 

There are two carbonated springs on the property. The principal 
one issues from crevices in mica schist on the side of a ravine 50 
yards above Mr. Garretson's cabin. It yields perhaps 1 gallon a 
minute of cold carbonated water and has been protected by a 
spring house, beside which there are minor seepages of carbonated 
water. Other carbonated seepages rise beneath the floor of the 
spring house and yield nearly as much as the main drinking spring. 
Considerable iron stains the overflow channel. 

The second spring is two-fifths of a mile westward and 50 yards 
from the bank of a creek that is tributary to the West Fork. The 
water rises in a board-curbed pool beneath a shed roof. It is about 
as strongly carbonated as the main spring and has nearly the same 
flow and temperature. Besides its use for drinking, water from 
this spring has been conducted in a wooden trough to a small tank 
30 yards away and heated for bathing. The water deposits iron at 
the spring and also seems to contain considerable calcium, for it 
deposits lime carbonate in the trough and in the heating tank. The 
spring is locally designated the ''salt spring," perhaps on account 
of its distinctly alkaline taste. Like the other spring, it issues 
from mica schist, which, however, is here covered with loamy soil. 
The schist, which is apparently associated with the sedimentary 
rocks of the region, is mineralized to some extent and has been pros- 
pected at a number of places. Half a mile northwest of the second 
of the Garretson springs two tunnels have been driven about 40 
feet into the canyon side on quartz veins. In one of them there is a 
salt that seems to consist mainly of iron sulphate, associated with 
pyrite. Quantities of this material have been collected by campers 
and used for preparing solutions for bathing wounds and even as an 



CARBONATED SPRINGS. 217 

eye wash and as a snuff for catarrh. Southward, across the canyon 
from the springs, there are abandoned quicksilver prospects. The 
Garrctson springs are sometimes referred to as Cinnabar Springs, a 
name that is derived from these prospects, but this name is misleading. 

KELLER SODA SPRING (SISKIYOIT 2). 

Keller Soda Spring, -ih miles below Garrctson Soda Springs, is on 
the north side of West Fork of Beaver Creek, 100 yards from and 100 
feet above the stream. It is near the homo of Mr. Alex. Keller, who 
ha'^> had a cabin and a small garden beside the creek since about 1902. 
A rock-wallod basin makes a small drinking pool in which the water 
is cool and strongly carbonated. The discharge flows down an iron- 
stained channel and over a conspicuous deposit of lime carbonate 10 
or 12 yards in diameter. A small amount of carbonated water also 
seeps from crevices in the rock at the creek edge, 150 yards down- 
stream. The rock at tliis locality is a coarse- textured quartzitic 
material with some gneissic and hornblendic phases. 

CARBONATED SPRINGS AT SODA BAR (SISKIYOU 3). 

On the western side of the main fork of Beaver Creek, at Soda Bar, 
within 3 miles of the Oregon line, are two small cool carbonated 
springs that have not been improved but are occasionally visited by 
hunters. 

CARBONATED SPRING AT EDGE OF BEAVER CREEK (SISKIYOU 4). 

A small carbonated spring rises at the eastern edge of Beaver Creek, 
opposite the Curtis ranch, which is 2 miles above its mouth. A small 
basin has been made by drill and hammer in the gneiss from wliich 
the spring issues, and a spring house protects it. When it is not 
flooded by surface water, the spring water is moderately carbonated. 
The rock is iron stained along the overflow channel, but the water is 
apparently not liighly mineraUzed. There is another small and 
unimproved carbonated spring on the same side of the channel a 
ndle farther upstream. 

CARBONATED SPRINGS NEAR LITTLE BOGUS CREEK (SISKIYOU 5). 

In the western portion of the lava-covered region in northern CaU- 
fornia there are two areas of considerable extent in which there are 
a number of carbonated springs. The northern area is in the north- 
ern part of Siskiyou County; the southern is near the Siskiyou- 
Shasta county line. (See p. 220.) 

The northernmost group in the first area is on the east side of Little 
Bogus Creek about 4J miles northeast of Ager. Tlie main springs 
here issue from basins in low carbonate mounds on a larger deposit of 
lime carbonate at the base of a hillside, near the county road between 



218 SPRINGS OF CALIFORNIA. 

Ager and Klamath Hot Springs (Siskiyou 7, p. 120). This deposit is 
about 75 yards in diameter and is built up prominently above the 
flat that borders the creek. Upon it there are six springs that yield 
small flows of carbonated saline water. The largest spring forms an 
oval pool 3 by 6 feet across and 2 feet deep, in which a temperature 
of 72° was recorded. Its discharge is about 2 gallons a minute. 
Another pool 10 inches in diameter also yields about the same amount 
of water, whose temperature is 76°. The other basins are small^ of 
less discharge, and of lower temperatures. There are three other low 
mounds in this area of lime carbonate. One of these is entirely 
extinct; the other two have only seepage flows from basins 3 or 4 
inches in diameter. 

On the hillside about 300 yards northeast of the main carbonate 
deposit there is a prominent mound which is nearly 100 feet in 
diameter and 10 feet high on its upper side. A shallow pool 5 feet 
in diameter that is situated on its top yields perhaps 2 gallons a 
minute of carbonated sahne water 74° in temperature. At the 
roadside, 50 yards below it, there is another low iron-stained mound 
from whose top there is a seepage flow of warm water similar to that 
of the other springs. White deposits on the hillside a short distance 
northward indicate that carbonated water formerly issued there 
also. 

Material from the deposit that was first described has been used 
on an adjacent portion of the wagon road, for the carbonate is easily 
loosened by pick and forms a road material that soon packs to a 
firm surface. 

The water has been used by range stock as a substitute for a salt 
lick, but it is too warm and too saline to be pleasant for drinking. 

Lava, probably basaltic, covers the slopes and forms characteristic 
flat-topped hills near by. The association of lava with thermal 
carbonated water that deposits a notable amount of lime carbonate 
seems to be exceptionally well shown at these springs. Their tempera- 
tures have warranted their indication as thermal-carbonated springs 
on Plate III (in pocket), but they are more noticeably carbonated 
than thermal. The sahne character of the water is also worthy of 
note. 

Marine beds of Cretaceous age have been described by Diller ^ as 
probably underlying the lava of this region, and it seems probable 
that the sahnity of the springs is derived from these sedimentary 
beds. This same suggestion was advanced to account for the sahne 
character of Morgan Hot Springs, near Lassen Peak. 

1 Diller, J. S., Tertiary revolution in the topography of the Pacific coast: U.S. Geol. Survey Fourteenth 
Ann. Kept., pt. 2, p. 423, 1894. 



CARBONATED SPRINGS. 219 

TABLE ROCK SPRING (SISKIYOU 9). 

Three carbonated springs on the northeast side of Shasta Valley- 
may be considered to be in the same general locaUty as those near 
Little Bogus Creek. Tli.e principal one is on the Terwilliger ranch, 
12 miles east of Montague. It is situated a few hundred yards north 
of Little Shasta River and near the northern base of a flat-topped 
liill known as Table Rock. During 1909 the water was placed on 
the market under the label "Table Rock Water." 

At this place there is a very low mound of lime carbonate about 
100 yards in diameter, from near the center of which the spring 
rises, mainly from an irregular fissure 12 feet long and 1 inch to 
30 inches wide, along which the water is continuously and vigor- 
ously bubbhng. This fissure has been protected by a concrete wall 
2^2 feet liigh. In a bottling house beside it water for bottling has 
been obtained by a hand pump from a basin or well 1 foot in diameter 
and 10 feet deep. Near the bottling house there is also a shallow 
bubbling pond, 8 or 10 yards across. The water is not notably 
thermal, as it has a temperature of only 65°, but otherwise its occur- 
rence is similar to that of the springs near Little Bogus Creek. It is 
more strongly carbonated, however, and much less salty, and it 
probably contains considerable iron, as it deeply stains its overflow 
channel. 

CARBONATED SPRING AT EDGE OF LITTLE SHASTA RIVER (SISKIYOU 8). 

Two miles downstream from Table Rock Spring, and half a mile 
east of Little Shasta post office, strongly carbonated water rises from 
lava gravel at the southern edge of Little Shasta River, 30 yards 
north of a low lava bluff. The spring yields about 8 gallons a minute 
of water, 57° in temperature. It rises clear but is said to become 
cloudy, probably from a small amount of precipitated iron, after 
being bottled for a short time. Considerable iron-stained, cemented 
gravel is exposed in a stream bank 50 to 100 yards above the spring, 
and indicates that carbonated water formerly issued farther up- 
stream. The spring has been protected by a short piece of heavy 
galvanized-iron casing, but it is in pasture land some distance from 
the road and has not been much used. 

MARTIN SODA SPRING (SISKIYOU 11). 

The third of the carbonated sprmgs near Shasta Valley issues on 
the ranch of Mrs. M. F. Martin, near the southern base of Table Rock, 
about a mile southward in a direct line from Table Rock Spring. 
The Martin spring rises in a cemented basin at the edge of a creek. 
Its water is clear, cool (55°), and strongly carbonated, but its yield 
is only about 1 gallon a minute. Like the water of the spring at the 



220 SPEINGS OF CALIFORNIA. 

edge of Little Shasta River, it is said to become cloudy on standing 
and it has been used only locally for drinking. 

A conical pile of lime carbonate that probably marks an old spring 
vent rises above a considerable deposit of the same material in a 
barnyard 75 yards east of the spring, and a few yards above the 
spring lime-cemented gravel is also exposed along the creek. Neither 
the Martin Spring nor the one on Little Shasta River is now depositing 
noticeable amounts of lime carbonate, but the deposit near the first- 
mentioned spring, and the lime-cemented gravel near each, suggest 
that they did so at a time when their waters were warmer than they 
are now. 

Besides its location in the lava near Table Rock, the position of 
Martin Soda Spring is of interest because the stream at whose edge 
it rises issues in full volume 50 yards upstream from the spring. 
This stream is mentioned later among the large cold springs. Its 
position with respect to the carbonated spring may be accidental, 
but it at least suggests that the cold water found an outlet through 
old channels of the earlier, presumably thermal, carbonated spring. 

SHASTA SPRINGS (SISKIYOU 22). 

Nearly all of the carbonated springs in the southern of the two gen- 
eral localities that have been mentioned as lying along the western 
side of the lava area in northern California are close to Sacramento 
River. Shasta Springs, which are commercially the most important 
ones in this locality, are at Shasta Springs station, on the east side 
of Sacramento River. They were first brought to general notice 
in 1887, during the construction of the Southern Pacific Raiboad 
along the river, and their commercial development was early begun. 
A cemented drinking fountain and a spring house have been built 
over the springs, so their direct source is no longer visible, but the 
following description of their improvement has been published : ^ 

The ground immediately around the springs was cleared and the surface removed 
to bedrock. * * * 

Numerous small springs were discovered in the exposed surface of the bedrock. 
All of these were carefully closed by the following method : The necks of bottles were 
broken off and placed over the points of gas and water leakage, and suiTounded with 
cement, so that the gas and water could escape through the bottle necks and allow 
the cement to harden. After the cement had set, the mouths of the bottle necks 
were corked and a heavy layer of cement spread over them. The object of this was 
to force everything into the main fissure. 

The main fissure of the Shasta Spring was arched over, with the exception of the 
principal vent, over which a concrete reservoir was built. This reservoir was divided 
into two compartments, the front being an open drinking basin for the use of the public, 
and the rear a hermetically sealed reservoir, the interior dimensions of which are 

1 Watts, W. L., Mineral springs in Siskiyou County: California State Mineralogist Eleventh Rept., 
pp. 449-450, 1893. 



CARBONATED SPRINGS. 



221 



about 3 feet in diameter and 6 feet in height. * * * From this chamber a pipe 
leads directly to a small structure in which the bottling machinery has been 
erected. * * * 

The follomng analysis shows that the water is characterized by 
primary and secondary alkalinity and primary salinity and contains 
a large proportion of magnesimn : 

Analysis of water from main spring, Shasta Springs, Siskiyou County, Cal. 
[Analyst, W. S. Haines. Authority, 13th Cal. Constituents are in parts per million.] 



Temperature 

Properties or reaction: 

Primary salinity 

Secondary salinity. . . 

Tertiary salinity 

Primary alkalinity. . . 

Secondary alkalinity . 

Tertiary alkalinity. . . 



W" C. (51° F.) 

18 



23 

59 

(?) 



Constituents. 



By 

weight. 



Reacting 
values. 



Sodium (Na) 

Potassium (K).. . 

Lithium (Li) 

Calcium (Ca) 

Magnesium (Mg). 
Iron ( 



i(Fe). 



Aluminum ( Al) 

Manganese ( Mn) 

Sulphate (SO,) 

Chloride(Cl) 

Bromide (Br) and iodide (I). 

Fluoride (F) 

Carbonate (CO,) 

Metaborate (BO;) 

Arsenate (AsOi) 

Phosphate (P0<) 



Carbon dioxide (CO;') Present 



447 
23 
Trace. 
Trace. 
349 
10 
2.5 
Trace. 
8.6 
312 
Traces. 
Trace. 
1,195 
9.9 
1.4 



19.43 

.59 

Trace. 

Trace. 

28.70 

.36 

.28 

Trace. 

.18 

8.79 

Traces. 

Trace. 

39.83 

.23 

.03 

.03 



2, 359. 2 



The springs issue at the base of the steep canyon side. Eastward, 
400 feet above the springs, the country opens to a gentle upward 
slope northward to Mount Shasta. A summer resort has been estab- 
lished on the plateau-like slope, directly above the springs. The 
grounds are reached by an inclined railway from the railroad station 
below, or by a zigzag path two-fifths of a mile long, up the canyon 
side. Much water rises in cold springs near the top of the canyon 
and cascades down the slope, near the path. 

At the east bank of the river, 200 yards below Shasta vSprings, and 
also on the west bank, 150 yards farther downstream, small carbon- 
ated springs have formed iron-stained deposits of lime carbonate. 
The Griffin onyx marble quarry, which has been mentioned in con- 
nection with the deposits at Tolenas and Kessler springs, consists of 
a vein of onyx marble about 5 inches wide, on the western side of the 
river a short distance below Shasta Springs. It has not been worked 
for a number of years. 



222 SPKINGS OF CALIFOElSriA. 

OXONE SPRING (SISKIYOU 23). 

Oxone Spring rises on the plateau-like slope nearly a mile east of 
the grounds of Shasta Springs resort and a few yards from a small 
creek channel. It forms a pool 10 feet in diameter and 18 inches 
deep, in quartz and lava gravel that covers the surface.' Much gas 
continually rises in large bubbles in the pool. It is probably carbon 
dioxide, for it repeatedly extinguished a lighted newspaper held 14 
inches above the open water surface. The spring has been known 
locally for many years as Poison Spring, for it is said that birds and 
small animals are occasionally found dead beside it, having probably 
been overcome by the carbon dioxide. This is probably the spring 
that has also been i-eferred to as Scott Springs.^ 

The water is very strongly carbonated and has a pungent odor and 
a "sharp" taste, both of which characteristics are possibly derived 
from free carbonic acid. The spring has very little overflow directly, 
but it has been piped to the railroad station and there issues in a 
spring house 150 yards south of Shasta Springs. It flows quietly into 
a cement basin, but it there effervesces and tastes nearly as strongly 
carbonated as it does at the spring. 

CASTLE SPRINGS (SISKIYOU 19). 

About 300 yards west of Shasta Springs small carbonated springs 
rise near the southern bank of Sacramento River, which here makes 
a short eastward bend and then resumes its southerly course. These 
springs were early kno\vn as Castle Springs, and were at one time 
improved to slight extent as a resort. In 1909, however, the place 
had evidently been abandoned for many years. Four small carbon- 
ated springs were found, 5 to 15 yards apart, within a few yards of 
the river's edge. The northernmost one of these has a noticeably 
sulphureted as well as a carbonated taste, but another near it is only 
pleasantly carbonated. Each of these two springs yields perhaps 
2 gallons a minute. The southern two springs have only seeping 
flows. One of them deposits considerable iron; the other has a 
strongly carbonated and slightly acidic taste. This is one of the tnree 
carbonated springs in the State that was observed to have an acidic 
taste, the other two being Oxone Spring and one at the southwest 
edge of Clear Lake. The taste is possibly due to the presence of 
free carbonic acid. 

The springs rise in gravel and soil that border the river, but the 
bowlders along the stream and the rocks of the canyon side ai-e of 
lava, probably andesiticj like that near Shasta Springs. 

1 California State Mineralogist Eleventh Kept., p. 452, 1893. 



CARBONATED SPRINGS. 223 

WARMCASTLE SODA SPRINGS (SISKIYOU 28). 

Six miles in a direct line east of Shasta Springs is another group 
of carbonated springs, known as Warmcastle Soda Springs. The 
place is If miles south of McCloud lumber mills and was formerly 
conducted as a resort, but it has been deserted since about 1903. 
In 1909 a 20-room frame hotel still stood on the grounds. 

The principal spring, which is about 125 yards east of the hotel, 
rises in a concrete, dome-covered basin beneath a spring-house roof, 
and from a pipe at one side discharges about 10 gallons a minute of 
cool, strongly carbonated water. A small bubbling pool makes a 
marshy patch near this spring, and toward the hotel, beside a wagon 
road, another carbonated spring rises in a box-curbed basin. Its 
yield is perhaps one-half gallon a minute. Five hundred yards north- 
ward, beside a stream that rises from marshy land near by, a fourth 
carbonated spring issues through a joint of tile pipe and yields perhaps 
4 gallons a minute of moderately carbonated water. All four of the 
cai'bonated springs deposit small amounts of iron, but they do not 
seem to be otherwise strongly mineralized. The main spring is much 
used by travelers along the road, and is also a favorite drinking place 
for the children from a schoolhouse 200 yards eastward. 

The springs rise on the forested plateau surface near the southern 
base of Mount Shasta. The rock is lava, probably basaltic, which 
has weathered sufficiently to form red soil over most of the surface, 
but it is exposed at numerous places along stream channels and road 
cuts. 

There are said to be other carbonated springs that are undeveloped 
on Bear Creek, which is a number of miles northward from the 
Warmcastle springs. 

UPPER SODA SPRING (SISKIYOU 26). 

Upper Soda Spring is three-fourths of a mile northward across 
Sacramento River from Dunsmuir, at the base of low lava hills, 150 
or 200 yards from the river, which here makes a short eastward bend 
in its southerly course. The spring has been known for perhaps 
half a century by several names, of which Campbells Soda Spring 
and Freys Soda Spring are most common. The place has been con- 
ducted as a resort for a number of years, and the bottled water has 
a local market. The water rises in a cement basin in a small house 
and is thence piped to a botthng house near by, outside of which a 
faucet has been placed for pubhc use. The water is cool, moderately 
carbonated, and is apparently not notably mineraUzed. 



224 SPEINGS OF CALIFORNIA. 

CAVE SPRING (SISEIYOU 25). 

Cave Spring is near the eastern edge of Sacramento River and 
about one-half mile north of Upper Soda Spring. It issues from a 
crevice in the rock at the base of a 25-foot cHff of dark-colored lava, 
beneath which is the small cave from which the spring takes its 
name. It has been used only as a drinking spring. Like Upper 
Soda Spring it is cool and moderately carbonated, but it apparently 
contains more iron than the former, as it has deeply stained its 
overflow channel. 

TWIN SPRINGS (SISEIYOU 24). 

About 200 yards north of Cave Spring two small carbonated 
springs rise about 4 yards apart in joints of tile pipe. They are 
known as Twin Springs, and, like Cave Spring, are used only for 
drinking. The water deposits considerable iron, but it does not 
seem to be highly mineralized. Like Upper Soda and Cave springs, 
Twin Springs rise near the base of a low lava bank. The lava is 
also exposed across the river to the south and northward upstream , 
but on the western side of the canyon, opposite Twin and Cave 
springs and for some distance above and below them, light-colored 
dioritic rock is exposed.^ This material may have had some influ- 
ence in furnishing a place of upward escape for the carbonated water. 

CASTLE CRAG SPRING (SHASTA 2). 

Castle Crag Spring was formerly known as Lower Soda Spring and 
also as Hibbs Soda Spring, but during recent years the property 
has been improved as a resort under the name of Castle Crag 
Farm, and the spring has come to be best known by the newer 
name. It is situated at the base of a bank near the southern edge 
of Soda Creek, 5 miles south of Dunsmuir and a mile east of Sacra- 
mento River. A number of years ago a stone and concrete spring 
house was built over the spring, and the water formerly overflowed, 
from a cement basin in its center. When the spring was visited, 
however, the water stood at about the ground level in this basin 
but rose vigorously in a small open pool 5 yards away, as if from a 
break in the supply pipe. The water is strongly carbonated and 
deposits considerable iron. It is said that it has never been placed 
on the market but has been used only at the spring. The following 
analysis shows that it is a strongly alkaline-sahne water: 

I This rock has been examined microscopically by E. S. Larsen, jr., and found to contain granular augite 
and secondary hornblende, chlorite, biotite, calcite, and sericite. 



CARBONATED SPRINGS. 



225 



Analysis of ivater from Castle Crag Spring, Shasta County, Cal. 

[Analyst, Thomas Price & Son. Authority, Register of Mines, California Min.Bur. Constituents are in 

parts per million.] 



Temperature 

Properties of reaction: 

Primary salinity 

Secondary salinity 

Tertiary "salinity 

Primary alkalinily 

Secondary alkalinity 

Tertiary alkalinity 

Constituents 

Sodium (Na) 

Potassium (K) 

Lithium (Li) 

Ammonium (NH^) 

Barium ( Ba) 

Calcium (Ca) 

Magnesium (Mg) 

Iron(re) 

Aluminum ( Al) 

Manganese (Mn) 

Chloride (CI) 

Bromide (Br) 

Iodide (I) 

Carbonate (CO3) 

Metaborate (BO2) 

Arsenate ( AsOi) 

Phosphate (PO4) 

SUica (Si02) 

Carbon dioxide (CO2) 



12° C. (53° F.) 

41 



21 



By 
weight. 



Reacting 
values. 



1,155 

28 

.5 
15 
.7 
207 
258 
7.8 
3.6 
.4 
1,198 

.9 
Trace. 
1,493 
Trace. 
.9 
Trace. 
84 



50.20 

.72 

.07 

.83 

.01 

10.30 

21.20 

.28 

.40 

.01 

33.82 

.01 

Trace. 

49.77 

Trace. 

.02 

Trace. 

2.78 



4,452.8 



Present. 



Present. 



The rock that is exposed along the road from the river to a place 
350 yards southeast of the spring is dark-colored lava, but at this 
place a green diabase is exposed, which forms a bank that extends 
below the road to the spring and for some distance beyond. At the 
roadside 200 yards southeast of the spring there are also small car- 
bonated seepages from this rock. 

CAEBONATED SPRING ON SODA CREEK (SHASTA 3). 

At the north side of Soda Creek, 1^ miles above Castle Crag Spring, 
a small carbonated spring issues in a little pool in the stream gravel, 
between two bowlders of the green diabase, which persists at least 
this far up the canyon. 

The water is clear and moderately carbonated and deposits small 
amounts of lime carbonate and iron. Along the bank of the creek, 
about 150 yards below the spring, a lime carbonate deposit is exposed 
for a few yards. 

The spring has not been improved, but it has been visited by picnic 
parties. It is also used as a roadside drinking spring, as it is only 50 
yards from an automobile road that follows the canyon of Soda 
Creek. 



35657°— wsp 338—15- 



-15 



226 



SPRINGS OF CALIPOENIA. 



There are said to be other small carbonated springs on a branch of 
McCloud River several miles eastward . 

CASTLE ROCK SPRINGS (SHASTA 4). 

Castle Rock Springs rise along the side of Sacramento River 5 
miles west of south from Dunsmuir. One spring, which formerly rose 
in the eastern edge of the river, has been protected by a concrete wall, 
the ground about it has been filled in, and i>art of its flow now issues 
in a cemented drinking basin. The water is pleasantly carbonated 
and also has a distinct taste and odor of hydrogen sulphide. Bottled 
water from this spring has been marketed since about 1903. It is 
pumped by water power to a bottUng house at the west side of the 
river, beside the railroad, and is passed over a series of slate plates 
to aerate it and thus remove the hydrogen sulphide before bottUng. 
The following analysis shows the water to be primary alkaline sahne 
and secondary alkaUne, like that of the other principal springs in the 
locality: 

Analysis of water from main spring, Castle Rock Springs, Shasta County, Cal. 
[Analyst, Thomas Price & Son. Authority, advertising matter. Constituents are in parts per million.] 



Properties of reaction: 

Primary salinity 

Secondary salinity 

Tertiary salinity 

Primary alkalinity 

Secondary alkalinity 

Tertiary alkalinity 

Constituents 

Sodium (Na) 

Potassium ( K) 

Lithium (Li) 

Bai'ium (Ba) 

Calcium (Ca) 

Magnesium (Mg) 

Iron (Fe) 

Aluminum ( Al) 

Manganese (Mn) 

Chloride (01) 

Carbonate (CO3) 

Silica (Si02) 

Carbon dioxide (CO2) 

Hydrogen sulphide (H2S) 



43 


23 
34 
3 



By 
weight. 



Reacting 
values. 



16 



127 
133 



771 
870 



2,745.0 



Present. 
Present. 



33.32 

.41 

.02 

Trace. 

6.34 

10.94 

.01 

1.35 

.01 

2L74 

29.32 

1.63 



Present. 
Present. 



Two other carbonated springs are situated on the western edge of 
the river 100 yards above the main spring. One of these has been 
protected by a joint of tile pipe and the other by a board curbing. 
Both are moderately carbonated and have been used as drinking 
springs. 

Castle Rock Springs issue from dark-colored lava, probably basaltic, 
that here forms the bed of the river as well as its banks and is the 
extension down the river of a narrow lava flow from Mount Shasta. 



CARBONATED SPRINGS. 227 

This lava overlies slates that probably furnish the saline constituents 
of the several carbonated sprin.o;s of the locality. 

CARBONATED SPRING NEAR CASTLE CREEK (SHASTA 5). 

A small carbonated spring rises near the west edge of Sacramento 
River about three-fourths of a mile south of Castle Rock Springs and 
60 yards below the mouth of Castle Creek. It has been j)rotected by 
a joint of tile pipe and forms a local drinking spring. Like the main 
spring at the Castle Rock group, its water tastes distinctly sulphureted 
as well as carbonated, and hence it is often spoken of as a sulphur 
spring. 

CARBONATED SPRING IN HOT SPRING VALLEY (PLUMAS 2). 

A carbonated spring issues in Hot Spring Valley about one-half mile 
west of Drake Hot Springs (Plumas 4, p. 142) that is of interest both 
because of its position and its amount of flow. The spring is in 
meadowland a few yards north of Warner Creek and yields about 8 
gallons a minute of moderately carbonated water. It has been pro- 
tected by a board curb and a log fence, and its water is occasionally 
used for drinking but is too warm (83°) to be palatable. Bubbles 
that are probably of carbon dioxide continually rise in the pool, and 
the water deposits considerable iron, but it does not taste very 
noticeably minerahzed. 

CARBONATED SPRING NORTH OF SOUPAN HOT SPRINGS (SHASTA 14). 

About 1^ miles north of Soupan Hot Springs (Shasta 15, p. 141) 
there is a carbonated spring that was used as a drinking spring 
when the sulphur deposits at those springs were being prospected, 
but lately it has not been often visited. Like the carbonated spring 
in Hot Spring Valley (Plumas 2), it is of interest, however, in con- 
nection with the hot springs near by, and its presence indicates that 
much of the bubbhng at Soupan Hot Springs and at Bumpass Hot 
Springs (Shasta 16, p. 140) is caused by carbon dioxide.^ 

CARBONATED SPRINGS ON SPANISH CREEK (PLUMAS 14). 

At the north end of the Sierra Nevada, in Plumas County, there 
are a number of carbonated springs, those best laio\vn being beside the 
road between Quincy and Greenville, whore lime carbonate has been 
extensively deposited at two localities. The southern locality is on 
the eastern side of the canyon of Spanish Creek, about 10 miles by 

1 A "cold soda lake" is indicated on some early maps of this locality, its position being shown about 1 
mile north of Bumpass Hot Springs. Such a lake was not foimd when the locality was visited in 1910 
and was not known to several people who are familiar with the locality. It is possible that conditions 
have changed since the early maps were made and that the carbonated spring north of Soupan Hot Springs 
is near the place indicated. The activity at Lassen Peak, beginning May 30, 1914, indicates that the 
positions of the springs on its slopes have varied in the past. 



228 SPRIISrGS of CALIFOElSriA. 

road northward from Quincy. One small carbonated spring here 
forms a drinking pool at the upper edge of the road, and 20 yards 
south of it, below the road, there is a second spring or group of springs. 
At the latter place three small board-curbed basins have been made, 
and the discharge was formerly piped to a bathhouse 30 yards far- 
ther down a steep slope. When visited in 1909 this house had evi- 
dently been unused for a considerable time, and a crumbly layer of 
lime carbonate one-fourth of an inch thick had been deposited on 
the floor by the overflow from the bath tub. 

The carbonate deposit covers the surface from the springs west- 
ward to the creek, a distance of 125 yards down the steep slope, and 
forms a bluff for an equal distance along the stream. A few other 
deposits of much smaller extent were observed on the western side 
of the creek. 

CARBONATED SPRINGS ON INDIAN CREEK (PLUMAS 13). 

About Ij miles in a direct line northward from the springs on 
Spanish Creek that have just been described, carbonated springs 
issue on the southeastern side of Indian Creek, near a deposit of 
lime carbonate formed between the road and the creek. This 
deposit is larger than that at the other locality, for it covers an 
area of approximately 200 by 400 yards and forms a steep slope for 
a quarter of a mile along the creek. Plate IX, B (p. 134), shows a 
lower portion of this deposit. The carbonate deposit extends north- 
ward parallel to a bend of the creek at this locality and makes a 
low ridge that slopes northward to the stream. Along the crest of 
this ridge there are three depressions or sinks, 5 to 30 yards in 
diameter, in which a hard compact lime carbonate is exposed which 
resembles that of the "hoodoos" near Mammoth Hot Springs in 
Yellowstone Park. In the southernmost sink, which is the largest, 
two mounds of the more common white lime carbonate have been 
formed, and small pools of carbonated water of seeping flow still 
exist on their tops. Small veins of calcite and of banded onyx mar- 
ble were also noticed in the darker, more massive carbonate in this 
sink. The more recent surficial deposits on the lower slopes are of 
the usual white carbonate. At the southern edge of the deposit, a 
few yards below the road, two pools form drinking springs, and the 
water has also been taken away in bottles for its supposed medicinal 
value. It is moderately carbonated, but it is too warm and too 
saline and calcic to be a pleasant drinkmg water. These pools are 
about 4 feet apart and are approximately a foot in diameter and a 
foot deep. When visited they did not overflow and contained only 
a few inches of water. On bailing out one the other was also emp- 
tied, indicating that they are connected underground. 

A few small springs were noticed at the northern end of the deposit 
and also along its western side, bordering the creek, but only two of 



CAEBONATED SPRINGS. 



229 



thorn had an approciahio flow. Each of thoso yioldod porjiaps 1 
galh)ii a miiiuto. One of them issued horizontally, with considerable 
force, among lime-cemented bowlders at the creek side. The small 
flow is worthy of remark in connection with the size of the deposit. 

The rocks of this region are slates and sandstones, with some 
quartzitic material, that are very probably of the same series that 
has been maj^ped by Dillor,^ 3 or 4 miles westward, and by Turnor,^ 
2 or 3 miles southward, as the Calaveras formation, of Carboniferous 
age. 

Although no lava was observed near the springs, the southeastern 
border of the lava area that surrounds Lassen Peak is only about 10 
miles to the west. The massive and hoodoo-like character of the 
underlymg portion of the deposit makes it seem not improbable that 
the springs were thermal and accomplished most of their work of 
deposition during or shortly following the eruptions from Lassen Peak, 
and that they represent one phase of the results of volcanic activity 
when that mountain was in the making. 

ARLINGTON SPRINGS (PLUMAS 12). 

There are two carbonated springs near the Arlington Bridge, at 
the southeastern edge of Indian Valley, 3 J miles in a direct line 
northwest of the carbonated springs on Indian Creek. One of the 
Arlington Springs, as they are locally known (though the name Bach 
Sprmgs has also been applied to them), rises in a barrel at the road- 
side; the other issues from a short piece of 1-inch pipe, on the gentle 
hill slope 25 yards to the southeast. Both yield cool, pleasantly car- 
bonated water. The following partial analysis shows the water to be 
chiefly of secondary alkaline character: 

Analysis of ivater from main spring, Arlington Springs, Plumas County, Cal. 
[Analyst, G. E. Colby (1906). Authority, owner of springs. Constituents are in parts per million.] 



Proyjerties of reaction: 

Primary salinity 


( 


10 


Secondary salinity 










Primary alkalinity 


3 


Secondary alkalinity 


87 


Tertiary alkalinity 


?) 






Constituents. 


By 
weight. 


Reacting 

values. 


Calcium (Ca) 


• 


} 235 

Small. 

33 

23 

365 

100 

Small. 

799 

Present. 




Magnesium (Mg) 


11.77 


Iron (Fe) 


Small. 


Sulphate (SO^) 


.69 


Chloride (CI) 


.66 


Carbonate (CO3) 


12.18 


Combined water 




Silica (Si02) 


Small. 


Totalsolids 




Carbon dioxide (CO2) 


Present. 







1 Diller, J. S., U. S. Geol. Suryey Geol. Atlas, Lassen Peak folio (No. 15), 1895. 

2 Turner, H. W., U. S. Geol. Survey Geol. Atlas, Downieville folio (No. 37), 1897. 



230 



SPRINGS OP CALIFOENIA. 



Although hon was not determmed quantitatively in the analysis, 
the water probably contains a relatively large proportion of this 
element, for it has iron stained the soil in an area perhaps 75 yards in 
diameter to such an extent that it has been used locally as a paint 
pigment. Considerable lime carbonate has also been deposited in 
this area, but it is so deeply iron stained that it is not conspicuous. 

CARBONATED SPRING IN HUMBUG VALLEY (PLUMAS 9). 

A small carbonated spring rises in Humbug Valley a short distance 
from the little settlement of Longville. Although the spring is only 
locally known, its water is much appreciated during the summer, as 
it is pleasantly carbonated and makes a palatable drinking water. 
There is said to be another similar spring beside the road between 
Longville and Keddie station on the Western Pacific Railway. 

CARBONATED SPRINGS ON CHIP CREEK (PLUMAS 10). 

On Chip Creek, several miles farther south, there are carbonated 
springs similar to the one in Humbug Valley. As they are not on a 
main traveled road, they have been seldom visited and have been 
known only locally. 

MOUNT IDA SPRING (BUTTE 3). 

Mount Ida Spring is situated about 6 miles east of OroviUe, in a 
wide ravine, at the base of slopes of schistose rock. The analysis 
below shows that the water is primary saline and secondary alkahne. 

Analysis of water from Mount Ida Spring, Butte County, Cal. 

[Analyst, G. E. Colby (1892). Authority, 13th Cal. and owner of spring. Constituents are in parts 

per million.] 



Temperature 

Properties of reaction: 

Primary salinity 

Secondary salinity 

Tertiary salinity 

Primary alkalinity 

Secondary allf alinity 

Tertiary alkalinity 

Constituents. 

Sodium (Na) 

Potassium (K) 

Lithium (Li) 

Strontium (Sr) 

Calcium (Ca) 

Magnesium (Mg) •. 

Iron (Fe) 

Manganese (Mn) 

Sulphate (SO4) 

Cliloride (Cl) 

Carbonate (CO3) 

Metaborate (BO2) 

Phosphate (PO4) 

SUica (SiOz) 

Carbon dioxide (CO2) 



18° C. (65° F.) 

62 
3 


35 
94 



By 
weight. 



Reacting 
values. 



166 

25 

Trace. 

Trace. 

76 

14 

5.9 

Trace. 

279 

88 

138 

Trace. 

4.1 

35 



7.23 

.64 

Trace. 

Trace. 

3.78 

1.16 

.21 

Trace. 

5.80 

2.49 

4.60 

Trace. 

.13 

L17 



831.0 



10.59 



CAEBONATED SPRINGS. 



231 



The spring was well known to the Intlians and later to white set- 
tlers, and formerly supplied a small th'inking pool. As this pool 
easily became roiled, however, a number of yeai*s ago a shaft was 
sunk 13 feet deep to bedrock at the spring, and a joint of pipe was 
cemented into the fissure from which the water came. The water 
rises in this pipe to the surface clear and fresh and is used locally as a 
table water. It was at one time bottled at the Oroville soda works. 

SUMMIT SODA SPRINGS (PLACER 6). 

A number of groups of small ciu-bonated sprmgs lie m the Sierra 
west of Lake Tahoe. One of the northernmost of these groups has 
long been known as Summit Soda Springs, although the springs are 
about 13 miles by road south of Summit station, on the Southern 
Pacific Railroad. The springs are situated m a little flat beside 
North Fork of American River, and in the late eighties or early 
nmeties a hotel was built, and the place was conducted as a resort 
for several years. The hotel burned in 1898, however, and since 
then the property has not been open to the public. 

Fom* cool carbonated sprmgs rise in the flat on the south side of 
North Fork, and a fifth rises at the edge of the stream. Three 
of them have been inclosed by spring houses and are used as drinking 
springs. All have small flows, but they are strongly carbonated and 
deposit noticeable amounts of iron. The following analyses of one 
of the principal springs shows the water to be moderately alkaline 
and saline: 

Analyses of water from main spring, Summit Soda SpriJigs, Placer County, Cal. 
[Constituents are in parts per million.] 





1 


2 


Properties of reaction: 

Primary salinity 


34 


13 
53 
328 




36 


Secondary salinity 





Tertiary salinity 





Primary allcalinitv 


14 


Secondary alkalinity 


50 


Tertiary alkalinity. .. . ... 


339 






Constituents. 


By 
weight. 


Reacting 
values. 


weight. 


Reacting 
values. 


Sodium (Na) 


238 

8.0 
210 

20 

22 

10 

272 

201 

Trace. 

33 


10.34 

.20 

10.48 

1.64 

.79 

1.11 

7.69 

15.76 

Trace. 

1.09 


248 
Trace. 

183 
21 
23 
16 

272 

143 


10.76 


Potassium (K) 


Trace. 


Calcium (Ca) 


9.14 


Magnesium (Mg) 


1.73 


Iron(Fe) 


.82 


Aluminum (Al) 


1.77 


Chloride (CI) 


7.69 


Carbonate (CO3) 


13.94 


Metaborate(B02) 




Silica (SiOs) 


35 


1.16 








1,014 




941 










Carbon dioxide (CO2) 


1,593 


72.41 


1,586 


72.09 







1. Analyst and authority, Winslow Anderson (1888). 

2. Analyst, J. F. Rudolph (1878). Authority, U. S. Geol. Survey Bull. 32. 



232 SPRINGS OF CALIFOENIA. 

On the hillside 200 to 500 yards southward, there are four other 
carbonated springs which have been developed only to the extent of 
excavating small basins about them. 

The main springs issue in an area of granitic rock; the minor ones, 
on the hillside to the southeast, issue from schists that are a result of 
contact metamorphism between the granitic rock and slates. A mile 
southward the slopes are covered with andesitic lava, and Tinker 
Knob, 3 miles to the east, is a volcanic mountain.^ 

Near the road, 2 miles westward, downstream from the Summit 
springs, there are considerable deposits of lime carbonate, and small 
quantities of carbonated water still seep from a few points. North 
of the railroad, on the wagon road to Truckee, there are also carbon- 
ate deposits that are the work of mineral springs. 

FLORENCE SPRING (PLACER 6). 

A quarter of a mile northeast of Summit Soda Springs, on the 
northern side of the stream, there is a carbonated spring that is locally 
called Florence Spring. It has a considerably larger flow than the 
springs of the Summit group and is not so strongly carbonated, but 
it tastes of iron and deposits much iron along its overflow channel. 
The spring has not been improved, but it has been used to some 
extent for drinking. 

HEATH SODA SPRINGS (PLACER 4). 

Carbonated springs, known as Heath Soda Springs, issue on the 
north side of the canyon of North Fork of American River, 5 miles 
in a direct hne west of Summit Soda Springs. They yield con- 
siderably more water than the Summit Springs but are not so strongly 
carbonated. They have not been improved, and as the place is not 
easily accessible it is rarely visited. The springs issue in an area of 
granitic rock, within a quarter of a mile of the western border of an 
area of altered slates. Andesitic lava covers the slopes 2 miles north- 
ward and westward. 

CARBONATED SPRING NEAR SERENO CREEK (PLACER 3). 

About 3 J miles south of Soda Springs station, a short distance east 
of the road, is a small carbonated spring that forms a drinking pool. 
It is on the eastern side of the canyon of Sereno Creek, near the base 
of steep slopes of andesite overlying rhyolitic lava. 

DEER PARK SPRINGS (PLACER 7). 

In the canyon of Bear Creek, 8 miles in a direct line southeast of 
Summit Soda Springs, four small springs form drinking pools of cool, 
mildly carbonated water that deposits considerable iron. They were 

lA detailed description of the geology of this region is given by Waldemar Lindgren, U. S. Geol. Sur- 
Yey Geol. Atlas, Truckee folio (No. 39), p. 5, 1897. 



CAEBONATED SPRINGS. 



233 



formerly known as Scott Springs but are now known as Deer Park 
Springs. The place has been conducted as a resort since the 
eighties. In 1909 a hotel, a dining hall, and seven cottages provided 
accommodations for 150 guests. The buildings are situated in a 
little fiat on the northwestern side of Bear Creek, and the springs are 
on a hillside 150 to 200 yards eastward, across the stream. Small 
rustic houses have been erected over the springs, two of which are 
beneath one roof. Two of them are known as Soda springs, one as 
the Sulphur Spring, and one as the Iron Spring. Their waters have 
the distinctive tastes indicated by these designations and differ some- 
what though not markedly in composition, as is shown by the follow- 
ing analyses of three of them, all secondary alkaline, primary saline 
waters. 

Analyses of water from Deer Park Springs, Placer County, Cal. 

[Analyst, G. E. Colby (1909). Authority, owner of springs. Constituents are in parts per million.] 



Soda No. 1. 



Soda No. 2. 



Sulphur. 



Properties of reaction: 

Primary salinity 

Secondary salinity . . 
Tertiary salinity — 
Primary alkalinity. . 
Secondary alkalinity 
Tertiary alkalinity . 



Constituents. 



By 
weight. 



Calcium (Ca) 

Magnesium (Mg) 

Sulphate (SO4) 

Chloride (Cl) 

Carbonate (CO3) 

Silica (Si02) 

Total solids 

Carbon dioxide (CO2) 

Hydrogen sulphide (HjS) . 



\ 160 

174 

45 
297 

76 

990 

Present. 



Reacting 
values. 



By 

weight. 



7.99 

3.62 
1.27 
9.90 
2.52 



Present. 



205 

84 
39 

367 
31 

900 
Present. 



Reacting 

values. 



By 
weight. 



10.29 

1.75 

1.09 

12.23 

1.03 



Present. 



114 

111 

32 

210 

53 

670 

Present. 

Present. 



Reacting 
values. 



5.69 
2.31 



6.99 
1.76 



Present. 
Present. 



The springs rise in a small area of granitic rock which probably 
forms the core of the mountains to the west. At the springs the rock 
is decomposed to gravel and to kaolin-like clay. It is nearly sur- 
rounded by andesitic lava, which covers the slopes less than 100 
yards east of the springs and the surrounding area for several miles. 

CARBONATED SPRING NEAR MOUTH OF POWDERHORN CREEK 

(PLACER 11). 

A small cool carbonated spring lies near the mouth of Powderhorn 
Creek, 5 J miles in a direct line southwest of Deer Park Springs, but 
it is unimproved and is known mainly to hunters and fishermen. 
Small carbonated springs of similar character probably issue at 
other places in this region, but they are of little note and are known, 
chiefly to the local sportsmen. 



234 



SPRINGS OF CALIFOENIA. 



RUBICON SPRINGS (ELDORADO 3). 

Eubicon Springs form one of the oldest places of resort in the 
Lake Tahoe region, as they were visited in the sixties, when there 
was only a pack trail leading to them. The springs are in a little 
flat on the east side of Rubicon River, 12 miles by road westward 
from Lake Tahoe. In 1909 there was a small hotel and three log 
cabins on the property, and the place was open to guests during the 
summer months. A rustic spring house has been built over the 
principal spring, which rises at the base of a low granitic hummock 
or ridge at the edge of the flat. Like most other carbonated springs it 
is of small flow, the yield being only about half a gallon a minute. The 
water is cool, strongly carbonated, and is much prized for drinking. 
It tastes noticeably of iron and has deposited considerable iron along 
its overflow channel. As the following analysis shows, it is a primary 
and secondary alkaline water: 

Analysis of ivater from main Rubicon Springs, Eldorado County, Cal. 
[Analyst, N. E. Wilson. Authority, owner of springs. Constituents are in parts per million.] 

Properties of reaction: 

Primary salinity 

Secondary salinity 

Tertiary salinity 

Primary alkalinity 

Secondary alkalinity 

Tertiary alkalinity 




Constituents. 



Sodium (Na) 

Lithium (Li) 

Calcium (Ca) 

Magnesium (Mg). 

Iron (Fe) 

Aluminum (Al).. 
Sulphate (SO4)... 

Chloride (CI) 

Carbonate (CO3). 
Silica (SiOz) 



Carbon dioxide (CO2) . 



Attempts to bottle the water on a small scale have been unsuc- 
cessful because many of the bottles were broken by the carbon dioxide 
and others were so stained by iron as to injure the sale. 

About 100 yards north of the main spring, along the border of the 
granitic outcrop, a carbonated spring that yields perhaps twice as 
much water, rises in a rock-waUed basin and is used to some extent 
for drinking. About 200 yards farther north, downstream, another 
small carbonated spring issues at the base of a pine tree near the 
river, but it has not been improved. A fom-th carbonated spring, 
which has been known as Potter Spring, is three-quarters of a mile 
south of Rubicon Springs, at the southern edge of the meadow along 



CARBONATED SPRINGS. 235 

the river. It issues from a ere vice in massive granitic rock, 15 icvt 
above the level of llie meadow, and like the other springs it is strongly 
carbonated and has deeply iron stained its channel, but its yield is 
very small, being perhaps one-eighth of a gallon a minute. Therc^ is 
another seeping How, of little importance, 50 yards northeast of 
Potter Spring, at the edge of the meadow. 

For some distance south of this meadow the river flows northward 
toward it through a small, rocky gorge, in which, 100 yards above 
Potter Spring, there is a pothole in the massive granitic rock. A 
small amount of carbonated water apparently rises in this basin from 
a crevice beneath the rounded bowlder that it still contains, for the 
water in the pothole is rendered turbid by iron in suspension. 

The distinctly ferruginous character of the water at Rubicon 
Sprmgs is noteworthy in connection with the fact that they are sur- 
rounded for several miles by the massive iron-bearing granitic rock 
that is classed as a granodiorite.^ The slopes on each side of the 
river are largely devoid of soil and present an unusually good example 
of the granitic slopes of the Sierra. 

WENTWORTH SPRINGS (ELDORADO 2). 

Wentworth Springs are 5 miles in a direct line (8 miles by road) 
westward from Rubicon Springs m a small area of open land near 
Gerle Creek. The property was at one time claimed by a settler, 
and in 1909 a house still stood in the flat, but for several years the 
place has been only a small campers' resort. It has been visited 
mainly by people from Auburn and other towns to the west. 

At this locality two groups of small sprmgs issue along a small 
wash that is tributary to Gerle Creek. At the lower group six natural 
basins in an outcrop of schistose rock receive seeping flows of car- 
bonated water from crevices in the rock. Two of the basins — those 
chiefly used— have been protected by a fence railing and a board 
roof. The water in one of them is distinctly sulphureted, and all 
apparently contain considerable amounts but different proportions 
of salts in solution, as they differ noticeably from each other in taste. 
Chemical examination of water from the principal spring has shown 
the presence of abundant sodium, calcium, and magnesium and 
chloride and carbonate, as well as notable amounts of carbon dioxide 
and hydrogen sulphide. About 250 to 300 yards eastward, up the 
creek, eight other carbonated seepages discharge to small basins, 
in two of which sections of tile pipe have been sunk so as to form 
drinking pools. All of the springs of this group deposit considerable 
iron and noticeable amounts of lime carbonate. Like the lower 
springs they issue from schistose rock that is the result of contact 

1 Lindgren, Waldemar, U. S. Geol. Survey Geol. Atlas, Truckee folio (No. 39), 1897. 



236 



SPRINGS OF CALIFOENIA. 



metamorphism between the granitic rock on the east and the slate 
that is exposed for a couple of miles westward. 

GLEN ALPINE SPRINGS (ELDORADO 4). 

Glen Alpine Springs are reached by road 7 miles southward from 
Tallac, a resort at the south end of Lake Tahoe. The springs are 
said to have been discovered in 1867 by Mr. N. Gilmore, hence the 
place is sometimes known as Gilmores Glen Alpine Springs. The 
property has been conducted as a mountain resort since the eighties. 
In 1909 accommodations for 100 guests were provided in cottages 
and tents that were grouped beside Glen Alpine Creek, in a little 
flat that is bordered by steep, rocky slopes. 

The main spring rises near the center of the flat, in a protecting 
spring house, and forms a convenient and valued drinking place. 
The water is cold and strongly carbonated and deposits some iron 
along its overflow channel. The following analysis shows it to be an 
alkaline water, with a rather high content of iron and aluminum: 

Analysis of water from mainspring, Glen Alpine Springs, Eldorado County, Cal. 
[Analyst and authority, Winslow Anderson (1888). Constituents are in parts per million.] 



Temperature 

Properties of reaction: 

Primary salinity 

Secondary salinity 

Tertiary salinity 

Primary alkalinity 

Secondary alkalinity 

Tertiary alkalinity 

Constituents. 

Sodium (Na) 

Potassium (K) 

Calcium (Ca) 

Magnesium (Mg) 

Iron ( Fe) 

Aluminum (Al) 

Sulphate (SO4) 

Chloride (01) 

Carbonate (CO3) 

Metaborate (BO2) 

Silica (Si02) 

Carbon dioxide (CO2) 



4°C. (40° r.) 
19 

a 


26 
55 
150 



By 
weight. 



Reacting 
values. 



382 

Trace. 

329 

49 

15 

13 

49 

214 

917 

Trace. 

43 



16.61 

Trace. 

16.44 

4.04 

.53 

1.44 

1.03 

6.03 

30.56 

Trace. 

1.42 



2,011 



The water was bottled in small amount for one or two summers, but 
it was not found suitable for the purpose, possibly because of the iron 
content. 

Another carbonated spring, that is of somewhat greater flow than 
the main one, rises beside the spring house, but it has not been im- 
proved. Both it and the main spring apparently issue from a crev- 
ice in the granitic rock beneath the shallow alluvium of the flat. Seep- 
ages in the creek bed 150 yards eastward have iron stained the stream 
gravel, and carbonated water probably rises at that place also. 



CARBONATED SPRINGS, 



237 



The springs rise near the eastern border of a small area of granitic 
rock in a rather comi^lex region consisting of an igneous bedrock 
series that contains detached masses of slate and its accompanying 
schistose metamorphic phases.^ 

LAMBERT SODA SPRINGS (TUOLUMNE 1). 

In the central part of the Sierra, near the crest of the range and 
about 100 miles south of the Lake Tahoe region, there is another 
region in which a number of carbonated springs rise. The northern- 
most of these that are worthy of note are the Lambert Soda Springs, 
near Tuolumne River, about 25 miles by trail and road northeast from 
Yosemite Valley. 

The springs rise at the northern edge of Tuolumne Meadows, about 
125 yards nortli of the river's edge, at the upper border of a grassy 
slope. There is only one spring of appreciable flow, but water bubbles 
from numerous vents near by. The spring rises in a funnel-shaped 
pool about 14 inches in diameter in a little log cabin that protects it. 
In August, 1909, it yielded about 1 gallon a minute, but its discharge 
is said to vary somewhat. The water is clear, strongly carbonated, 
and effervescing, but considerable iron is deposited in the pool. Within 
the cabin there are also two small vents of inappreciable discharge 
marked by bubbhng. Six other similar pools, a few inches in diame- 
ter, lie on a low mound of iron-stained lime carbonate beside the 
cabin, and another group of eight small pools is located 15 to 25 
yards northeast of the cabin. The water in all of the pools is carbo- 
nated, and small amounts of iron and of lime carbonate are deposited 
at nearly all of them. Efflorescent soda salts also appear in the adjoin- 
ing grassy land. The following analysis shows the water to be pri- 
mary and secondary alkaline in character: 

Analysis of water from main spring, Lambert Soda Springs, Tuolumne County, Cal. 
[Analyst and authority, F. M. Eaton (1909). Comtituents are in parts per million.] 



Temperature 

Properties of reaction: 

Primary salinity 

Secondary salinity. . . 

Tertiary salinity 

Primary aLkalinity . . 
Secondary alkalinity . 
Tertiary alkalinity.. 



C. (47° F.) 

n 





36 

53 

7 



Constituents. 



By 

weight. 



Reacting 
values. 



Sodium (Na) 

Potassium (K)... 

Calcium (Ca) 

Magnesium (Mg). 

Iron(Fe) 

Aluminum (Al).. 
Sulphate (SO4)... 

Chloride (Cl) 

Carbonate (CO3) . 
Silica (Si02) 



229 
5.3 

190 
20 

6.2 

24 

66 

564 

58 



9.96 

.14 

9.81 

1.64 

.22 

.49 

1.87 

18.80 

1.93 



1,168.5 



Carbon dioxide (CO2) . 



Present. 



Present. 



1 The rocks of this region have been described and mapped by Waldemar Liadgren, U.S. Geol. Survey 
Geol. Atlas, Pyramid Peak folio (No. 31), 1896. 



238 SPEINGS OF CALIFOElSriA. 

The springs have been used mamly for drinking by campers and 
travelers through this portion of the mountains, but they form one of 
the best-known groups of carbonated springs in the Sierra. The 
water has occasionally been used in making biscuits without the use of 
baking powder, as the carbon dioxide in the water serves to hghten 
them. 

The region is one of massive granitic rock, where domes and sharp 
spires are common weathering forms of the coarse-textured material. 

CARBONATED SPRING AT HEAD OF AGNEW MEADOV/S (MADERA 3). 

A number of small carbonated springs are situated in the drainage 
basin of the northern branches of San Joaquin River, which lies south- 
ward across the divide from the headwaters of Tuolumne River. The 
springs are rather isolated from one another, but several of them are 
near trails through this rugged section of the mountains and are becom- 
ing well known as drinking springs to the rapidly increasing number 
of people who appreciate the grandeur of the high Sierra and visit 
them during the summer. 

At the northern end of Agnew Meadows, about 20 miles in a direct 
line (or 28 miles by road and trail) southeast from Lambert Soda 
Springs, there is a low, iron-stained mound of lime carbonate near 
some prospect dumps. Very little water issues here now, but the 
alkaline deposits are said to be used by deer as a salt lick. 

CARBONATED SPRING NEAR PTJMICE FLAT (MADERA 4). 

A carbonated spring that is often visited by travelers is situated 
about 4^ miles by trail southward from the spring at the head of 
Agnew Meadows and one-fifth of a mile from the main trail in Pumice 
Flat, northwestward up the eastern side of Middle Fork of San Joaquin 
River. A cool, rather stagnant pool, a yard in diameter, Hes 30 
yards from the stream, on a gentle slope that is covered "v\dth pumice 
gravel. Across the stream there is a bluff of dark lava agglomerate. 
The water is strongly carbonated, and considerable iron is deposited 
along its seepage overflow. Near the river's edge, 50 or 75 yards west- 
ward, there are several small pools that are slightly carbonated, but 
they seem to be supplied mainly by seepage water from the river. 
There is said to be another small carbonated spring a quarter of 
a mile farther upstream, however. 

CARBONATED SPRING ON MINARET CREEK (MADERA 2). 

A smaU but strongly carbonated spring lies in the canyon of Minaret 
Creek, about 5 miles westward by trail from the spring near Pumice 
Flat. In 1909 a well- traveled trail had not been opened along Minaret 
Creek, however, and the spring had been seldom visited. 



CARBONATED SPRINGS. 239 

CARBONATED SPRINGS IN SODA SPRING FLAT (MADERA 5i. 

Two miles south of tlio spriui;- nonv Piiinicc^ Flut is a itkvuIow known 
as Soda Spring Flat, which is a favorite camping place witJi fishermen 
because of its nearness to the river and the good camping facilities 
that it affords. On its western side, at the bank of a creek that joins 
th(^ river a short distance farther down, there is a small carbonated 
spring that is well known to campers. It yields perhaps 2 gallons a 
minute of cool, strongly carbonated water. A small pool 12 yards 
farther downstream yields a seeping flow of distinctly carbonated 
water. About the same distance northwestward, upstream from the 
main spring, there is another small pool of slightly carbonated water. 
Two other larger pools, that are sunk below the turf of the meadow 
and are 100 and 150 yards northward from the main spring, also con- 
tam distinctly carbonated water, and the gravel in them is stained 
with iron. 

The waters in the upper two of the small pools issue from soil and 
gravel along the stream bank, but tiiat in the lower one issues directly 
from a bank of columnar lava that is exposed for some distance along 
the canyon, beneath higher slopes of granitic rock. The columnar 
character of the lava is exceptionally well shown half a mile south of 
the springs, at the Devils Post Pile, where it forms a bluff. 

The association of the carbonated springs with lava was referred 
to in the description of Reds Meadows Hot Springs (Madera G, p. 55), 
which are about 1\ miles southeast of Soda Spring Flat. The asso- 
ciation is worthy of mention again here, although the same close 
relation of lava to the existence of carbonated springs was not 
observed at all of the carbonated springs in the high Sierra. 

CARBONATED SPRING IN FISH VALLEY (FRESNO 1). 

At the eastern end of Fish Valley, 7 miles in a direct line (nearly 
11 miles by trail) southward from Soda Spring Flat, a carbonated 
spring forms a pool 2^ feet in diameter about 20 yards east of the 
trail and 4 yards east of a large pine tree at the base of a granitic 
knoU. The water is cool, strongly carbonated, and deposits some 
iron, but there is only a seeping flow. A small amount of lime car- 
bonate has been deposited around the basin, and 25 yards eastward 
on the side of the knoll there is a low mound of the material 10 yards 
across. No water now issues from the mound, but it was evidently 
deposited at a former outlet of the spring. The rock of this region is 
massive granite and forms a cliff south of the spring that compares 
favorably in height with the lesser cliffs of Yosemite Valley. 



240 SPEINGS OF CALIPOENIA. 

CARBONATED SPRINGS ON MIDDLE FORK OF SAN JOAQUIN RIVER 

(MADERA 10). 

A number of iron-stained lime carbonate deposits and carbonated 
seeping springs are situated on the north side of Middle Fork of San 
Joaquin River above the mouth of Cargyle Creek, 7 miles westward, 
downstream from the spring in Fish Valley and 3 miles above the 
Miller Bridge. They are in a steep portion of the canyon, however, 
and are difficult to reach, so that they have been seldom visited. 

CARBONATED SPRING ON NORTH FORK OF SAN JOAQUIN RIVER 

(MADERA 9). 

Near Sheep Crossing, 2^ miles in a direct line northwest of the 
carbonated springs on Middle Fork of San Joaquin River, a short 
distance below the bridge that here crosses North Fork of the San 
Joaquin, on the western side of the stream and on the trail south- 
westward from Reds Meadows, is a spring that, like the others, is 
cool and strongly charged with carbon dioxide. Lava forms a prom- 
inent volcanic terrace along the eastern side of the stream and 
again suggests a relation between lava and carbonated water. 

CARBONATED SPRINGS ON EAST FORK OF GRANITE CREEK (MADERA 7). 

East Fork of Granite Creek is 3 or 4 miles west of North Fork of 
San Joaquin River and flows southward nearly parallel with it. A 
trail from the south follows up the northern part of the creek and 
thence swings westward across Isberg Pass and northward to Yo- 
semite Valley. Near the head of the creek is Sadlier Lake, at which 
a small meadow affords good camp grounds. On the western side 
of the creek, between it and the trail, small carbonated springs issue 
at two places that are respectively three-fourths mile and 1^ miles 
south of the lake. 

The upper spring issues from a crevice in massive granitic rock, 20 
yards west of the creek. Its water is strongly carbonated and a notice- 
able film — probably of lime carbonate — forms on a small pool below 
the crevice. The rock surface over which the water flows is iron- 
stained, and considerable areas of rock higher up the slopes are con- 
spicuously stained, as if by the same means at a former period of 
greater spring flow. 

At the lower place the spring rises among the bowlders and gravel 
of a small stream course, 15 yards east of the trail. The water 
apparently issues from four small vents and forms a shallow pool 
over whose surface a white filmy crust, probably of lime carbonate, 
collects. 

Like that of the upper spring, the water is strongly carbonated 
and has deeply iron stained its channel, but the flow is small. 



CARBONATED SPRINGS. 



241 



CARBONATED SPRING NEAR FOERSTER PEAK (MADERA 1). 

A small carbonated spring" rises near the southeastern base of 
Foerster Peak, about 3^ miles in a direct line northward from Sadlier 
Lake. It is not near a main trail, however, and has been seldom 
visited. 

CARBONATED SPRING NEAR BREEZE LAKE (MADERA 8). 

Near the northwest side of Breeze Lake, which is about 7 miles in 
a direct hne southwest of SadUer Lake, there is a small spring of cool 
carbonated water. It is occasionally visited, as it is less than half a 
mile from a trail through this part of the mountains. Many other 
cool carbonated springs of similar character are scattered through 
the liigh Sierra, but they are not generally Ivuown nor of particular 
interest. 

COBURN SODA SPRING (TULARE 9). 

In the southern part of the Sierra, along the branches of Tule and 
Kern rivers, are many carbonated springs, a few of wliich lie near roads 
or trails and have become known and used as drinking springs. 
Probably the best-known spring in this region is the one situated 
at Springville, 18 miles north of east from Portersville, in a lumber 
yard on the property of Mr. A. M. Coburn, on the north side of 
North Fork of Tule River, 15 yards from the stream. The spring 
rises in a cement basin beneath a shed roof. It forms a greatly 
prized drinking spring, though the water is rather warm (68°). 
Much gas continually rises with the water, which is moderately car- 
bonated and stains its run-off channel with iron. The following 
analysis shows that it is a rather strongly niineraUzed water, sec- 
ondary alkahne and primary saUne in character: 

Analysis of water from Cohum Soda Spring, Tulare County, Cal. 
[Analyst and authority, C. H. Stone (1906). Constituents are in parts per million.] 



Temperature 

Properties of reaction: 

Primary salinity 

Secondary salinity . . 

Tertiary salinity 

Primary alkalinity. . 
Secondary alkalinity 
Tertiary alkalinity.". 



20" C. (68° r.) 



Constituents. 



By 

weight. 



Reacting 
values. 



Sodium (Na) 

Potassium (K)... 

Calcium (Ca) 

Magnesium (Mg) . 

Iron(Fe) 

Aluminum (Al).. 
Sulphate (SO4)-.. 

Nitrate (NO3) 

Chloride (CI) 

Carbonate (CO3) . 
Silica (SiOa) 



539 

19 

179 

52 



21 



618 

618 

76 



23.43 

.49 

8.94 

4.25 

.48 

.45 

.00 

17.45 

20.60 

2.50 



2,135 



Carbon dioxide (CO2) . 



Present. 



Present. 



35657°— wsp 338—15- 



-16 



242 SPRI]SrGS of CALIFOEIsriA, 

In 1909 the water had not been placed on the market. 
The country rock of the region is granitic. The spring rises from 
a fissure in this rock, which was exposed when the bowldery gravel 
was cleared away, before constructing the present basin. Part of the 
fissure was closed by cement, in order to confine all of the discharge 
to one outlet. 

CARBONATED SPRING ON MIDDLE FORK OF TULE RIVER (TULARE 10). 

On the northern side of Middle Fork of Tule Kiver, about 6 miles 
east of Sprmgville and 1^ miles below the junction of the two main 
branches of the Middle Fork, is a small carbonated spring, to which 
a trail has been worn down the slope from the road a quarter of a 
mile above. The spring forms a small pool beneath a granitic bowlder 
20 feet above the stream. Besides being moderately carbonated, the 
water tastes faintly of hydrogen sulphide. A considerable deposit, 
which is deeply iron stained, has been formed at the spring, and iron 
and a small amount of lime carbonate are also deposited along the 
overflow channel. 

DOYLE SODA SPRINGS (TULARE 4). 

Doyle Soda Springs are on North Fork of Middle Fork of Tule 
River, 13 miles northeast of Springville. A flat on the west side of 
the stream furnishes a good camping ground, and the place has long 
been used as a camping resort. 

Two springs, each of v/hich yields about 1 gallon a minute of mod- 
erately carbonated water, form pools 2 or 3 feet across, beside a 
gneissic bowlder near the western bank of the stream, within 15 yards 
of the water's edge. A third spring, nearer the stream, issues from a 
crevice in granitic gneiss. Its water is strongly carbonated and 
spurts out intermittently from the rock. There is considerable iron 
stain near the spring vents. A small amount of carbonate of lime or 
magnesia is also deposited by the spray from the main springs, but 
the water is probably not highly mineraUzed. All of the carbonated 
water probably issues from the gneiss, which seems to form a belt in 
the granitic rock. 

CARBONATED SPRING ON SOUTH FORK OF MIDDLE FORK OF TULE 

RIVER (TULARE 11). 

A carbonated sprmg of unusually large flow rises on the northern 
side of South Fork of Middle Fork of Tule River about 2 miles above 
its junction with North Fork of Middle Fork. The yield of this 
spring was estimated at about 25 gallons a minute. The water is 
warm (77°), strongly carbonated, and tastes faintly sweetish, prob- 
ably of iron.- A deposit of lime carbonate that is much iron stained 
extends to the river's edge, which is normally about 5 yards away. 



U. S. GEOLOGICAL SURVEY 



WATER-SUPPLY PAPER 333 PLATE XIII 




.•1. JACKSON VALLEY MUD SPRINGS, MENDOCINO COUNTY. 
White patches are fog, not vapor from springs. 




B. GRIZZLY SPRINGS, LAKE COUNTY. 




C. NELSON SODA SPRINGS, TULARE COUNTY. 



CARBONATED SPRINGS. 243 

Although a number of other carbonated springs in this region arc 
also above a normal temperature, the unusually high temperature 
of this sprmg is especially worthy of note, and it is therefore indicated 
on Plate III (m pocket) as a thermal carbonated spring. The spring 
rises near the trail at the stream crossing, so it is used to some 
extent for drinking. The rock near it, as elsewhere along the canyon, 
is granitic. 

CARBONATED SPRING ON SODA CREEK (TULARE 12). 

About H niiles above the spring just described (Tulare 11) there 
is a carbonated spring on Soda Creek 150 yards above the trail. The 
spring issues among granitic ^"owlders at the eastern side of the stream 
channel. Like the springs farther downstream, it is strongly carbon- 
ated, tastes sweetish, and deposits iron, but a noticeable amount of 
Hme carbonate was not seen. The spring is \dsited to some extent 
for drinking water. 

NELSON SODA SPRINGS (TULARE 13). 

Nelson Soda Springs, or Camp Nelson, as the place is better known, 
is a mountam resort 15 miles east of Springville and near South Fork 
of ]\fiddle Fork of Tule River, also called the East Fork of Middle 
Fork. 

Four carbonated springs rise on the property. The lowest spring 
is on the southern bank of the stream, one-quarter of a mile west 
of south from the resort. It issues beneath an overhanging bank, 
in a small natural grotto of lime carbonate (PI. XIII, C) and flows 
over an iron-stamed terrace of the same material. The sprmg yields 
approximately 8 gallons a minute of strongly carbonated water, but 
it is too warm (69°) to be palatable. A second spring rises one-third 
of a mile southeast of the resort about 50 feet above and 50 yards 
from the north side of the river. It forms a small, rock-walled pool 
that yields about 4 gallons a minute of carbonated water 63° in tem- 
perature. It has deposited only a small amount of lime carbonate, 
but it has deeply iron stained its run-off channel. About 75 yards 
east of the spring just described another carbonated spring of nearly 
the same discharge issues on a low bank near the river in a deposit 
of lune carbonate that borders the stream for 200 yards. Two-fifths 
of a mile farther east a fourth spring rises in a little meadow. It 
yields about 8 gallons a minute of effervescing carbonated v/ater that 
is fairly cool (62°) and is the most palatable of the four. 

The springs rise in a region of granitic rock, but on the slopes above 
them are ledges of limestone that may account for the apparent high 
amount of calcium in their waters. 

Limestone appears, possibly as included masses in the granitic rock, 
at a number of other places in this part of the Sierra. Although its 



244 SPRINGS OF CALIFORNIA. 

outcrops were not observed to be so closely associated with the other 
carbonated springs as they are at Nelson Soda Springs, it seems 
plausible that masses which are not exposed furnish the calcium and 
carbonate constituents of some of the numerous other carbonated 
springs in the Sierra. There are many seeping carbonated springs 
and deposits of Ume carbonate along the banks of the South Fork of 
Middle Fork of Tule River, but all the noteworthy carbonated springs 
are behoved to be mentioned in the preceding descriptions. 

TULE RIVER SODA SPRING (TULARE 15). 

There is a carbonated spring on the Tule Indian Reservation, 16 
miles east of Portersville, that is known as Tule River Soda Spring. 
It is situated about 200 yards southwest of an old schooUiouse, at the 
north edge of South Fork of Tule River. It is submerged during 
periods of high water, but in the summer it forms a drinking spring 
that has been occasionally resorted to by picnic parties. The spring 
issues beneath a large granitic bowlder, from crevices in gneiss that 
is similar to the rock at Doyle Soda Springs. The main spring rises 
in a rock-waUed basin 2 feet square, but a number of vents in the 
gravel beside it are marked by bubbhng. The water is moderately 
carbonated and deposits considerable iron. 

CARBONATED SPRING NEAR MOUNTAINEER CREEK (TULARE 5). 

A small carbonated spring issues on rocky slopes near Mountaineer 
Creek, close to its junction with Peck Creek, about 25 miles by trail 
northeast of Springville. It is not easily accessible, however, and 
has not been often visited. 

CARBONATED SPRING IN LLOYD MEADOWS (TULARE 14). 

A cool carbonated spring in Lloyd Meadows, about 9 miles by 
trail east of Nelsons, is well known to campers and fishermen in that 
part of the Kern River region and is used as a drinking spring, but 
like other springs in the Sierra, the yield of water is not large. 

CARBONATED SPRING NEAR NORTH FORK OF KERN RIVER (TULARE 3). 

North Fork of Kern River flows in a deep canyon that widens to a 
walled vaUey in which is a spring that, probably because of the 
character of the valley, has been referred to as Little Yosemite Soda 
Spring.^ The spring is about 2| miles north of a small lake, known 
as Kern Lake, and 100 yards west of the river, at the lower edge of 
a meadow. The water rises in a rock-waUed pool 3 feet below the 
normal ground surface, at the base of a bank in the meadow soil. 
It is cool (51°), strongly carbonated, and deposits considerable iron. 
The following analysis shows that the water contains only a very 

1 Wheeler, G. M., U. S. Geog. Surveys W. 100th Mer. Arm. Kept., 1876, p. 195. 



CARBONATED SPRINGS. 



245 



moderate amount of solids in solution, being essentially primary and 
secondary alkaline in character: 

Analysis of ivater from carbonated sprinff near North Fork of Kern River, Tulare 

County, Cal. 

[Analyst, Oscar Loew (1876). Authority, Wheeler report. Constituents are in parts per million.] 



Temperature 

Propeities of reaction: 

Primary salinity 

Secondary salinity 

Tertiary salinity 

Primary alkalinity 

Secondary alkalinity 

Tertiary alkalinity 

Constituents 

Sodium (Na) 

Calcium (Ca) 

Iron (Fe) 

Sulphate (SO4) 

Chloride (CI) 

Carbonate (CO3) 

SiHca (Si02) 

Carbon dioxide (CO2) 



11° C. (52° F.) 

10 


SO 
40 
32 



weight. 



Reacting 
values. 



109 

64 

4.5 

Trace. 

28 

220 

73 



4.76 

. 3.20 

.16 

Trace. 

.80 

7.32 

2.42 



498. 5 



Excess. 



The rock of the valley sides is mainly granitic, the spring probably 
rising from the granitic bedrock that underlies the stream gravel and 
meadow alluvium. A mile northeastward, along Golden Trout Creek, 
are cliffs of lava, and 2^ miles in a direct line northeastward, at 
Natural Bridge, there is a large deposit of lime carbonate which has 
been referred to in the description of Jordan Hot Springs (Tulare 7, 
p. 53). It may be that the carbonated water of the present isolated 
spring in the valley bears some relation to the former carbonated 
springs at Natural Bridge, 1,600 feet higher, but the relation is not 
apparent. A fault that is considered to extend along this part of 
the course of Kern River may, however, have determined the point 
at which the carbonated water now issues. 



CARBONATED SPRING IN UPPER FUNSTON MEADOW (TULARE 1). 

In Upper Funs ton Meadow, about 13 miles by trail northward 
from Kern Lake, on a plateau lying between two branches of Kern 
River, a small spring furnishes cool, moderately carbonated water, 
and seems to be similar in character to the one near Kern Lake. 
It is known to campers and cattlemen in the region. 

CARBONATED SPRING NEAR QUINN HORSECAMP (TULARE 2). 

Quinn Horsecamp is about 9 miles in a direct line west of Kern 
Lake but 16 miles by trail over Coyote Pass. Near Soda Creek, 
which heads near the camp, there is a carbonated spring of consid- 
erable flow that is known to travelers over the trails in this region. 



246 



SPRINGS OF CALIFORNIA. 



CARBONATED SPRINGS IN MONACHE MEADOWS (TULARE 8). 

Carbonated springs rise in Monache Meadows, near South Fork of 
Kern Kiver, about 14 ixiiles by trail southwest of Olancha — a small 
settlement at the eastern base of the Sierra. Several trails enter 
these meadows, so the springs are well known to travelers through 
this part of the mountains, though the water is too warm to be pleas- 
ant for drinking and is distinctly sulphureted as well as carbonated. 
It issues near the eastern base of Monache Mountain, a rhyolite 
mass ^ that towers above the meadow. 



CARBONATED SPRING IN WELDON VALLEY (KERN 12). 

A small carbonated spring rises in Weldon Valley, about 10 miles 
northeast of Onyx post office and a short distance from the road that 
leads southeastward through Wa]ker Pass to the eastern front of the 
Sierra. The spring is not of importance for drinking, but like a num- 
ber of others it is of geologic interest because of its carbonated water 
and its isolated position. 

There are probably many other small carbonated springs in the 
region of the Sierra that is drained by Kern and Tule rivers, but those 
which have been mentioned are all that were learned of and are prob- 
ably all that are known to any extent. 

CARBONATED SPRINGS ON ENCINO RANCH (LOS ANGELES 8). 

A carbonated spring that rises on the Encino ranch, 14 miles north- 
west of Los Angeles, was early improved and made use of for bathing 
and irrigation. In 1875 it supplied a stone reservoir and a bathing 
pool and yielded about 5 gallons a minute of water 85° in tempera- 
ture.^ The following analysis shows it to be a primary and secondary 
alkaline and primary saline water of moderate mineralization: 

Analysis of water from main carbonated spring on Encino Ranch, Los Angeles County, 

Cal. 

[Analyst, Oscar Loew (1876). Authority, Wheeler report. Constituents are in parts per million.] 



Temperature 

Properties of reaction: 

Primary salinity 

Secondary salinity . . . 

Tertiary salinity ." 

Primary alkalinity. . . 
Secondary alkalinity . 
Tertiary alkalinity . . 



29° C. (85° F.) 

43 


24 
33 
20 



Constituents. 



weight. 



Reacting 
values. 



Sodium (Na) 

Potassium (K)... 

Lithium (Li) 

Calcium (Ca) 

Sulphate (SO4) . . 

Chloride (CI) 

Carbonate (CO3). 
Phosphate (PO4). 
Silica (SiOz) 



294 
Trace. 
Trace. 

129 

368 
18 

331 
Trace. 

115 



12.76 

Trace. 

Trace. 

6.43 

7.67 

.50 

11.02 

Trace. 

3.81 



1,255 



Carbon dioxide (CO2) 

Hydrogen sulphide (H2S). 



Excess. 
Trace. 



Trace. 



1 Reported by Adolph Knopf. 2 Wheeler, G. M., U. S. Geog. Surveys W. 100th Mer., 1876, p. 195. 



CARBONATED SPRINGS. 247 

In 1910 the spring still furnished the water supply for the ranch. 
Bubbles of inflammable gas rise with the water, which has a 
slight odor of hydrogen sulphide. A temperature of 84° was 
recorded in the reservou-. Another spring of weak flow rises about 
30 feet west of the main one and is also inclosed by a small stone 
reservoir. Its water is similar in character to that of the main 
sprmg. The water rises from Mocene shale, which here dips about 
25° N. toward San Fernando Valley. 

BUCKMAN SPRINGS (SAN DIEGO 17). 

In the southeastern part of San Diego County, 35 miles in a direct 
line but nearly 60 miles by road east of San Diego, is an isolated 
group of small carbonated springs, which were developed about 
1876 and have been improved for a number of years. The water 
has been marketed for table use under the label ''California Club 
Water." The group, which is known as Buckman Springs, com- 
prises six small carbonated springs, lying 20 to 30 yards apart on a 
gentle slope on the eastern side of Tia Juana Creek. One of the 
springs issues from pegmatite at the creek edge; another, 40 yards 
farther upstream, rises in a box-curbed pool at the base of a bank in 
the soil. These two springs have not been used commercially. The 
other four springs are arranged in a square, 25 to 50 yards east of the 
creek, and have been developed by excavating small reservoirs in low 
mounds of lime carbonate. The gas and water from them have been 
collected by tanks and piped to a bottling house over the largest 
spring. All of the flows are small, probably less than 1 gallon a 
minute, but the water is strongly carbonated and is pleasing for table 
use. The considerable amount of iron in the water has been detri- 
mental to its sale for table use, for a portion is deposited as a slight 
coating in the bottles after they have been filled for a few weeks. 

The rock near the springs is granitic and is cut by pegmatite dikes, 
but half a mile northeastward Mils of a dark-colored diabase that 
contains much hornblende and is cut by quartz ledges extend into 
the creek valley. The pegmatite in the granitic area and the horn- 
blende rock near by furnish conditions that differ somewhat from 
those observed at other carbonated springs. The presence of both 
rocks is at least worthy of note in connection with the unusually high 
contents of iron and silica that are indicated by an old analysis of 
the water. The high relative sahnity and unreasonably high '"' com- 
bined water" in this analysis, however, cast doubt on its reliability 
as reported. 

MAGNESIA SPRING (RIVERSIDE 13). 

In the southeastern desert section of California there are a fev,' 
springs that are noticeably carbonated as weU as being alkaline or 
saline like many of the other desert springs. 



248 



SPRINGS OF CALIFOEFIA. 



Magnesia Spring, which is situated in a canyon on the western side 
of Colorado Desert, about 15 miles west of Indio, yields a small 
amount of water that effervesces with carbon dioxide and is also locally 
beheved to contain a notable amount of magnesium. As the spring 
is about 2 miles from the main road along the west side of the desert 
and is reached only by a dim trail, it has not been often visited. 

McCAESr SPRINGS (IMPERIAL 4). 

McCain Springs are about 4^ miles southward from another group 
known as Soda Springs (Imperial 3), which are described among the 
saline springs (p. 303). The springs lie in a broad wash in an area 
whose surface is cut by many gulches, and issue on a low mound that 
has probably been built up by material blown upon it and retained 
by the moist soil. They discharge a small amount of slightly carbon- 
ated water. 

The following analysis shows the character of water from a small 
carbonated spring near McCain Springs and probably also indicates 
the general chemical features of the water from the McCain group. 
The high content of total solids, which are chiefly primary saline and 
secondary alkaline in character, is probably typical of several other 
springs in the southwestern part of Colorado Desert. 

Analysis of water from carbonated spring in Colorado Desert, Imperial County, Cal. 

[Analyst, W. O. Robinson (1909). Authority, United States Bureau of Soils. Constituents are in parts 

per million.] 



Properties of reaction: 

Primary salinity 

Secondary salinity . . . 

Tertiary salinity 

Primary alkalinity. . . 
Secondary alkalinity. 
Tertiary alkalinity . . . 



(?) 



Sodium (Na) 

Potassium (K) 

Calcium (Ca) 

Magnesium (Mg).. 
Sulphate (SO4)..-. 

Nitrate (NO3) 

Chloride (01) 

Carbonate (CO3) . . 
Metaborate (BO2)- 
Phosphate (PO4).. 



Constituents. 



By 

weight. 



1,628 

4 

436 

224 

68 



2,028 

1,549 

Trace. 





5,937 



Carbon dioxide (CO2) Present. Present, 



Reacting 
values. 



70.78 

.10 

21.75 

18.43 

1.42 

.00 

56.50 

51.65 

Trace. 

.00 



SUMMARY OF CARBONATED SPRINGS. 

Reasons for the existence of most of the hot springs of the State 
are suggested by the geology or topography of the surrounding coun- 
try, but there is little apparent cause for the rise of carbonated water 
at many of the places where it does issue. 



CARBONATED SPRINGS. 249 

Nearly all the carbonated springs are found in the sedimentary 
and nietamorphic rocks of the Coast Ranges north of San Francisco 
Bay, in the lava area in the northern part of the State, and in the 
granitic and nietamorphic rocks of the Sierra, but the character of the 
rocks appears to have little influence on the carbonated character of 
the springs. In the tabulated summary, therefore, they are grouped, 
as were the thermal springs, as impartially as possible, into general 
locahties, with respect, first, to the formation of notable carbonate 
deposits; second, to the presence of lava near by; and third, to the 
rock from which they issue, in order to show what evidence they fur- 
nish as to the effect of lava on the formation of spring deposits. 

The water of several of the springs at which there are deposits is 
cool, but the maximum temperature of most of them is noticeably 
above the normal. In the tabulated Ust of carbonated springs the 
10 locahties at which hot springs have formed deposits are included 
(in itahcs) in order to bring together those springs at which there 
are notable deposits. As noted in the summary of the hot springs 
(pp. 151-153) , most of these carbonate-depositing thermal springs issue 
from or near lava. 

In the descriptions of the hot springs it has been suggested that the 
gas at a few of the carbonated hot springs may possibly be derived 
from the deeper layers of the lava, for carbon dioxide is a large con- 
stituent of the vapors that are given off during volcanic eruptions, 
and it may plausibly be considered to be occluded in the lower portions 
of the lava flows. The same suggestion is offered to account for the 
carbon dioxide in several of the larger cool carbonated springs, but it 
is based only on the evidence that is furnished by the most vigorously 
effervescing springs, especially Oxone Spring and Table Rock Spring, 
both of which issue from lava. This evidence is, however, partly 
counterbalanced by that furnished by the Gas Spring, on the Bartlett 
Springs property (Lake 9, p. 200), which issues from altered sediments. 

The hst shows 29 general locahties having no deposit and 31 having 
a deposit but offers httle suggestive evidence as to the cause of depo- 
sition. The seemingly approximate equahty in the number of locah- 
ties in each group disappears if the mdividual springs are counted, as 
the totals are 119 springs without deposits and 45 sprmgs with de- 
posits. Of these 45 springs 21 issue from sedimentary or nietamor- 
phic rocks, 10 from granitic material, and 14 from or near lava. 

With the carbonated springs are tabulated the locahties learned of 
at wliich there are notable carbonate deposits that are probably of 
spring origin, for some of them are of interest in connection wdth 
existing springs. 



250 SPRINGS OF CALIFOENIA. 

Carbonated-spring localities. 

A. No notable deposit (29 localities). 

I. No lava near by. 

In sedimentary and metamorphic rocks. 

1 . Walters Mineral Springs. 
Samuel Soda Springs. 
Gaillaumes Soda Springs. 

2. Lytton Springs. 

Carbonated spring near Little Sulphur Creek. 

Alder Glen Springs. 

Duncan Springs. 

McDowell Springs. 

Carbonated springs near Feliz Creek. 

Carbonated springs on Russian River. 

Ornbauns Mineral Spring. 

Carbonated springs on Garcia River. 

Carbonated spring near Boonville. 

Sing'leys Soda Spring. 

Gobbis Soda Spring. 

Carbonated springs at Shoemaker Dell. 

Carbonated springs at Hazel Hill. 

Carbonated springs near Wendling. 

3. Baker Mineral Springs. 
Salmon Creek Mineral Springs. 
Carbonated sj)rings at Travelers Home. 
Carbonated spring on White ranch. 
Carbonated spring on Snider ranch. 
Carbonated spring southwest of Willits. 
Carbonated spring west of Willits. 
Carbonated spring in Big Basin. 
Carbonated springs near Long Valley Creek. 

4. Jackson Valley Mineral Springs. 
Jackson Valley Mud Springs. 
Cantwell Soda Spring. 
Petersons Mineral Spring. 

5. Witter Medical Springs. 
Saratoga Springs. 

Carbonated spring near northwest edge of Clear Lake. 

Lee Soda Spring. 

Carbonated spring in canyon of Scott Creek. 

Bynum Spring. 

England Springs. 

Adams Springs. 

Spiers Springs. 

6. Baker Soda Spring. 
Quigley Soda Springs. 

Carbonated spring near northeast side of Clear Lake. 
Carbonated springs on Wiley ranch. 
Allen Springs. 
Bartlett Springs. 
Hoppins Springs. 



CAEBONATED SPRINGS. 251 

Newman Springs. 

Hazel Sprinc:?. 

Royal Spring. 

Paramore Spring. 

Carbonated spring near ranger camp. 

Carbonated spring on Bear Creek. 

Morton Soda Spring. 

7. Cooks Springs. 

8. Ferndale Springs. 
Alum Rock Park Springs. 
Grant Spring. 

9. Madrono Spring. 
Coes Sirring. 

10. Garretson Soda Springs. 
Carbonated springs at Soda Bar. 
Carbonated springs at edge of Beaver Creek. 

11. Mount Ida Spring. 

In granitic rocks. 

12. Rubicon Springs. 
Wentworth Springs. 

Glen Alpine Springs (Eldorado Coiinty). 

13. Lambert Soda Springs. 

Carbonated spring at bead of Agnew Meadows. 
Carbonated spring on Minaret Creek. 
Carbonated springs on East Fork of Granite Creek. 
Carbonated spring near Foerster Peak. 
Carbonated spring near Breeze Lake. 

14. Coburn Soda Spring. 

Carbonated spring on Middle Fork of Tule River. 

Doyle Soda Springs. 

Carbonated spring on Soda Creek (Tulare County). 

Tule River Soda Spring. 

Carbonated spring near Mountaineer Creek. 

Carbonated spring in Lloyd Meadows. 

Carbonated spring near North Fork of Kern River. 

Carbonated spring in Upper Funston Meadow. 

Carbonated spring near Quinn Horsecamp. 

Carbonated spring in Weldon Valley. 

15. Carbonated springs on Encino ranch. 

16. Magnesia Spring. 
McCain Springs. 

IT. Lava near by. 

In sediments. 

1. Carbonated springs on Cole Creek. 
Carlsbad Springs. 

Bonanza Springs. 

In lava. 

2. Jacksons Napa Soda Springs. 
Congress Spring. 

3. Soda Bay Springs (small cemented-gravel formation). 

Carbonated springs at southwest edge of Clear Lake (small cemented-gravel for- 
mation). 

4. Shasta Springs. 



252 SPRINGS OF CALIFORNIA. 

Oxone Spring. 
Castle Springs. 
Warmcastle Soda Springs. 
Upper Soda Spring. 
Cave Sirring. 
Twin Springs. 
Castle Crag Spring. 

Carbonated spring on Soda Creek (Shasta County) (deposit a short distance 
downstream). 

5. Castle Rock Springs. 
Carbonated spring near Castle Creek. 

6. Carbonated spring in Hot Spring Valley. 
Carbonated spring north of Soupan Hot Springs. 

7. Carbonated spring near Sereno Creek. 

In metamorphic rocks. 

8. Mtna Springs. 

9. Astorg Spring. 

In granitic and metamorphic rocks. 

10. Carbonated spring in Humbug Valley. 
Carbonated springs on Chip Creek. 

11. Heath Soda Springs . 
Deer Park Springs. 

Carbonated spring near mouth of Powderhorn Creek. 

12. Carbonated spring near Pumice Flat (covered by thin layer of pumice). 
Carbonated springs in Soda Spring Flat. 

Carbonated spring on North Fork of San Joaquin River. 

13. Carbonated springs in Monache Meadows. 

B. Notable deposits (31 localities). 
I. No lava near by. 
In sedimentary and metamorphic rocks. 

1. Napa Rock Soda Springs; 79° F. 
Phillips Soda Springs; 68° to 76°. 

2. Tolenas Springs; 57°. 

3. Kessler Springs; 60° ±. 

4. Vichy Springs; 88° to 90°. 

5. Kinsner Soda Spring; 47° (deposit a short distance below). 

6. Glen Alpine Springs (Lake County); 50° ±. 
Highland Springs; 52° to 82°. 

7. Grizzly Springs; 70°. 

8. Oil Spring; 76°. 
Deadshot Springs; 65° to 79°. 

9. Dinsmore Soda Spring; 63° + . 

10. Hough Springs; 66°. 

11. Fonts Springs; 75°. 

12. Congress Springs; 60°. 
Azule Mineral Spring; 60°. 

13. Banes Soda Springs; 60° ±. 
Helms Soda Springs; 60° ±. 

14. Carbonated springs on Spanish Creek; 62° to 68°. 
Carbonated springs on Indian Creek, 57° to 68°. 
Arlington Springs; 53°. 



SULPHUR SPRINGS. 253 

In (granitic rocks. 
15. Keller Soda Sprincr; 53°. 

IG. Summit Soda Springs; 44° to '55° (deposit farther downstream). 
Florence Spring; 52° (deposit farther downstream). 

17. Carbonated spring in Fish Valley; 54°. 

Carbonated springs on Middle Fork of San Joaquin River; 55° + . 

18. Carbonated spring on South Fork of Middle Fork of Tule River; 77°. 
Nelson Soda Springs; 62° to 69°. 

19. Buckman Springs; 60° to 65°. 

20. Jordan Hot Springs; 95° to 123°. 

21. Bucl-ei/e Hot Springs; 140°. 

II. Lava near by. 
In granitic rocks. 

1. Reds Meadoivs Hot Springs; 90° to 120°. 

2. Gravers Hot Springs; 50° to 146°. 

In lava. 

3. Carbonated springs on Chalk Mountain; 70°. 
Alum Spring; 60°. 

4. Carbonated springs near Little Bogus Creek; 54° to 76°. 
Table Rock Spring; 65°. 

Carbonated spring at edge of Little Shasta River; 57° (cemented gravel nearby). 
Martin Soda Spring; 55° (carbonate deposit near by). 

5. Fales Hot Springs; 97° to 141°. 

6. Hot and tvarm springs near Bridgeport; 100° to 148°. 

7. Morgan Hot Springs; 90° to 200°. 

8. Drake Hot Springs; 123° to 148°. 

9. Casa Diablo Hot Springs and pool; 115° to 194°. 
10. Shaffer, Amedee, and Highrock springs; 86° to 204°. 

Carbonate deposits that are probably spring formations. 

In canyon of Kern River 25 miles north of Kernville, Kern County. 
At Natural Bridge, 7 miles east of north of Kern Lake, Tulare County. 
Two miles west of Summit Soda Springs, Placer County. 
South of Euers Valley, 10 miles northwest of Truckee, Nevada County. 
Alabaster Cave, 5 miles southeast of Auburn, Placer County. 

SULPHUR SPRINGS. 

DISTRIBUTION. 

The following descriptions of sulphur springs include chiefly those 
that are not markedly thermal. Many thermal springs that are 
noticeably sulphureted have been described among the hot springs. 
The distribution of all the sulphur sprmgs is, however, shown on 
Plate III (in pocket), which shows that they are found mainly through 
the Coast Ranges, being more plentiful in the region north of San 
Francisco Bay than in that to the south. They occur at only a few 
scattered points in the Sierra and in the deserts of the southeast- 
ern part of the State. 



254 



SPRINGS OP CALIPOElSriA. 



ST. HELENA WHITE SULPHIJR SPRINGS (NAPA 10). 

St. Helena White Sulphur Springs are situated in the canyon of 
Sulphur Creek, 2 miles southwest of the town of St. Helena. They 
form the nucleus of an old and formerly a well-known resort, but 
about 1904 the hotel was destroyed by fire, and in 1909 the improve- 
ments had not been extensively rebuilt. There were, however, 
cottages and an open screened dining room, furnishing accommoda- 
tions for about 25 people, and a small bathhouse near one of the 
springs. 

Analyses of water from St. Helena White Sulphur Springs, Napa County, Cal. 
[Constituents are in parts per million.] 





1 


2 


3 


4 


5 




25° C. (77° F.) 

83 

4 




13 
21 


21° C. (69° F.) 

59 




5 

36 
9 


32° C. (90° F.) 

82 

1 




17 

22 


30°C.(86° F.) 

80 

5 




15 
13 


21° C. (70° F.) 

63. 

1 


Properties of reaction: 
Primary salinity.. 
Secondary salin- 
ity 


Tertiary salinity. . . 
Primary alkalin- 
ity 



0' 


Secondary alka- 
linity 


35 


Tertiary alkalinity 


(?) 


Constituents. 


By 
weight. 


React- 
ing 

values. 


By 
weight. 


React- 
ing 
values. 


By 

weight. 


React- 
ing 
values. 


By 
weight. 


React- 
ing 
values. 


By 
weight. 


React- 
ing 
values. 




218 

23 

10 

2.0 

123 

260 

9.4 

29 

11 


9.48 
1.15 
.82 
.22 
2.56 
7.33 
.59 
.97 
.36 


136 
42 
15 
5.6 
83 
133 
Trace. 
113 
25 


5.91 
2.10 
1.23 

.62 

1.73 

3.75 

Trace. 

3.76 

.83 


207 
28 
6.8 


8.99 
1.40 
.56 


232 
29 
13 


10.05 
1.45 
1.03 


177 
49 
24 


7.70 




2.45 


Magnesium ( Mg) 

Aluminum ( Al) 


2.00 


Sulphate (SO4) 

Chloride (Cl) 


96 
251 
(xl9 

20 


2.00 

7.08 

1.20 

.67 


131 

280 

a 13 

32 


2.73 

7.90 

.84 

1.06 


149 
164 
a 12 
110 


3.10 
4.63 


Sulphide (S) 


.75 


Carbonate (CO3) 

Silica (SiOa) 


3.67 


















685.4 




552.6 




627.8 




730 




685 




Hydrogen sulphide 
(H2S) 


34 


2.01 


Trace. 


Trace. 


41 


2.38 


28 


1.64 


Trace. 


Trace. 







a Reported as sodium and calcium sulphides. Recalculated on assumption that 41 per cent is CaS and 
59 per cent NazS by comparison with analysis of spring No. 5. 

1. Spring No. 5. Analyst and authority, Winslow Anderson (1888). 

2. Spring No. 9. Analyst and authority, Winslow Anderson (1888). 

3. Spring No. 2. Anal'yst, J. Le Conte (1871). Authority, U. S. Geol. Survey Bull. 32. 

4. Spring No. 6. Analyst, J. Le Conte (1871). Authority, U. S. Geol. Survey BuU. 32. 

5. Spring No. 7. Analyst, J. Le Conte (1871). Authority, U. S. Geol. Survey BuU. 32. 

The group includes five noteworthy springs which issue v/ithin a 
space of 150 yards near the foot of the slope on the northeast side of 
Sulphur Creek. All these springs were formerly improved with 
brick basins, but when visited the northern two were the ones chiefly 
used. One of these formed a drinking pool that yielded about one- 
half gallon a minute of mildly sulphureted water. The northern- 
most spring, which is about 25 yards beyond the drinking spring, 
was surrounded by a cement reservoir and yielded warm, mildly 



SULPHUR SPRINGS. 255 

sulphureted water, which supplied the bathhouse below it. The 
central spring was formerly used as a bathing pool, but it had become 
filled with nuid and grown with tules. The two southern springs 
filled slightly used brick drinkhig basins. The southernmost spring 
apjieared to be the largest of the five, as a stream of about 4 gallons 
a mmute, which apparently came from it, issued at the creek edge a 
few yards away. A temperature of 83° was recorded at this spring. 
The water of the other sprmgs is also noticeably warm, so the 
springs are marked on Plate III (in pocket) as thermal sulphur, but 
they are best known as sulphur springs. 

The analyses on page 254 show that the waters are essentially 
prmiar}^ saline. The presence of sulphide sulphur is of interest, as 
this form of sulphiu* Is considered to be the most efficient medicinally'. 

The springs issue from crushed sandstone of the Franciscan forma- 
tion,^ which forms the hills of the locality. 

NAPA VICHY SPRING (NAPA 13). 

A small spring, whose water is moderately sulphureted, issues about 
3 miles east of north from Napa, on low slopes of tuff aceous lava that 
border the valley. The water rises in a cemented basin within a cir- 
cular, latticed spring house. It is piped directly to a bottling house 
near by, where it is carbonated and bottled in siphons for local sale. 
It has been on the market since about 1898 as Napa Vichy Water. 

VALLEJO WHITE SULPHUR SPRING (SOLANO 2). 

Vallejo White Sulphur Spring is situated in the hills 4 miles north 
of east from Vallejo. The property has been conducted as a resort 
for a number of years, the improvements in 1909 including a hotel, 
several cottages, and a small artificial lake. 

The spring rises in a shallow pool about 12 feet in diameter, at the 
base of a steep, craggy slope of siliceous rock that has been mapped 
as being a portion of the Franciscan formation.^ The water is dis- 
tinctly sulphureted, but is not otherwise noticeably mineraUzed. A 
partial analysis, published in advertising matter, indicates that sodium 
and magnesium are the two principal constituents and that they are 
present in the ratio of 1 to 1.6. It is rather warm for drinking, as its 
temperature is 68°, but it is heated for batliing. It has also been 
bottled to some extent and marketed locally for table use. 

EL TORO SPRING (MARIN 1). 

Mildly sulphureted water issues at El Toro Spring on the eastern 
side of a basaltic hill 2^ miles northwest of Novato. This water was 
formerly bottled and sold for table use, but for a number of years it 

1 Weaver, Charles, U. S. Geol. Survey Geol. Atlas, Napa folio (unpublished). 



256 



SPRINGS OF CALIFORNIA. 



has been used only for domestic purposes. The spring rises in a 
stone basin, and its yield, which is about 4 gallons a minute, is piped 
to a storage tank 100 yards away, near the house. The following 
analysis indicates that the water is essentially primary alkaline and 
carbonated : 



Analysis of water from El Toro Spring, Marin County, Cal. 
[Analyst, W. T. Wenzel. Authority, 11th Cal. Constituents are in part per million.] 



Properties of reaction: 

Primary salinity 

Secondary salinity . . 
Tertiary salinity — 
Primary alkalinity. . 
Secondary alkalinity 
Tertiary alkalinity. . 



28 



54 

18 

367 



Constituents. 



By 
weight. 



React- 
ing 
values. 



Sodium (Na) 

Potassium (K) 

Calcium (Ca) 

Masnesium (Mg) 

Iron(Fe) 

Aluminum (Al) 

Sulphate (SO4) 

Chloride (CI) 

Carbonate (CO3) 

Carbon dioxide (CO2) 

Hydrogen sulphide (H2S) 



67 

11 
4.4 
5.7 
1.4 
.4 
8.6 

32 

84 



214.5 



315 
Present. 



2.92 
.29 
.22 
.47 
.05 
.04 
.18 
.91 

2.81 



14.31 
Present. 



O'DONNELL'S SPRINGS (SONOMA 17). 

Two sulphur springs of relatively small flow that issue in a ravine 
on the west side of Sonoma Valley have been used for drinking for a 
number of years, and of late a small sanitarium has been established 
at the place. The water is not strongly minerahzed, however, and 
the occurrence of the springs is not of unusual interest. 

TAYLOR SULPHUB, SPRING (SONOMA 13). 

A small sulphur spring, that is known as Taylor Sulphur Spring, 
lies at the base of the hills 2 miles southeast of Santa Rosa. A 
hotel was built on the property in 1870 and the place was opened as 
a resort, but the building burned within a few years. It was later 
rebuilt, mth accommodations for sixty people, and was conducted 
intermittently as a resort until the time of the earthquake of April 
18, 1906. It was again reopened as a resort in the summer of 1910, 
as Kawana Sulphur Springs but is probably best known by its 
original name. The water rises in a cement basin beneath a small 
spring house and yields perhaps 1 gallon a minute of faintly sul- 
phureted water. The hillside back of the spring is soil covered, but 
it apparently consists of lava, such as is exposed in the hiUs farther to 



SULPHUR SPRINGS. 



257 



the southeast. The following analysis shows the chief properties to 
be primary and secondary salinity: 

Analysis of water from Taylor Sulphur Spring, Sonoma County, Cal. 
[Analyst and authority, Wiaslow Anderson (1SS6). Constituents are in parts per million.] 



Temperature 

Properties of reaction: 

Primary salinity 

Secondary salinity 

Tertiary salinity 

Primary alkalinity 

Secondary alkalinity 

Tertiary alkalinity 

Constituents 

Sodium (Na) 

Potassium (K) 

Calcium (Ca) 

Magnesium (Mg) 

Iron (Fe) 

Aluminum (Al) 

Sulphate (SO4) 

Chloride (CI) 

Carbonate (CO3) 

Metaborate (BO2) 

Silica (Si02) 

Carbon dioxide (CO2) 

Hydrogen sulphide (H2S) 



16° C. (60° F.) 

56 
28 


16 
35 



By 
weight. 



Reacting 
values. 



93 
6.3 
7.0 
35 
Trace. 
8.4 
220 
59 
35 
Trace. 
20 



483. 7 



4.04 

.16 

.35 

2.88 

Trace. 

.93 

4.59 

1.67 

1.17 

Trace. 

.66 



1.61 
2.50 



WALL SPRINGS (SONOMA 10). 

Wall Springs are situated on the side of a large ravine near the 
northern border of the valley of Russian River, 14 miles northwest 
of Santa Rosa. The property has been improved for a number of 
years as a resort, accommodations being provided in 1909 by a small 
hotel and three cottages. 

Five springs issue near the buildings, in cemented basins 10 to 30 
yards apart, at the bases of small banks on the slope. They are 
designated, respectively, as Potash, Sulphur, Magnesia, Clearwater, 
and Iron springs. When they were seen all were probably diluted 
with surface water, but the Potash Spring tasted distinctly alkaline 
and the Sulphur and the Magnesia springs were noticeably sulphureted; 
the other two had no distinctive taste. Water from the Sulphur 
Spring has been piped to a tank near by and has been heated for 
bathing. The other springs have been used only for drinking. All 
apparently yield flows of less than 1 gallon a minute. Their re- 
corded temperatures ranged from 47° in the Clearwater Spring to 
63° in the Sulphur Spring. Although their flows were so slight and 
their basins were about equally exposed to the weather, the noticea- 
bly higher temperatures of the distinctly minerahzed springs indicate 
that the chemical changes that cause their mineraUzation also pro- 
duce observable amounts of heat. 
35657°— wsp 338—15 17 



258 SPRINGS OF CALIFOENIA. 

The rocks of the region are shales and sandstones, which are in 
some places considerably silicified, but the springs apparently 
issue from soft sandstone that overHes a bed of harder sedimentary 
material. Their small flows indicate that they are supplied by 
water of essentially surface origin, which becomes slightly mineral- 
ized from the shales and sandstones and is brought to the surface 
on the side of the ravine by a bed of relatively impervious material. 

SITLPHUR SPKINGS IN FRANZ VALLEY (SONOMA 12). 

Franz Valley lies about 15 miles north of Santa Rosa, between 
that place and Calistoga. Two small sulphur springs in it are 
occasionally used as drinking springs by outing parties to the Petrified 
Forest, a small group of sihcified tree trunks a few miles distant. The 
springs are probably similar in character to those at Mark West Warm 
Springs (Sonoma 11, p. 115), which are a few miles westward. Small 
undeveloped sulphur springs issue at a number of other places in the 
counties north of San Francisco and San Pablo bays. Among them 
is one in Lucas Valley, a few miles northwest of San Rafael, but it 
has b'een known only locally and is seldom visited. 

SULPHUR SPRING NEAR LITTLE SULPHUR CREEK (SONOMA 6). 

Near Little Sulphur Creek, about 7 miles northeast of Geyserville, 
on property that has been open for a few years as a summer resort 
under the name of Geyser Peak Ranch, is a spring that yields a small 
flow of cool, distinctly sulphureted water. It has been used only 
for drinking. 

The rocks at this locality are the shales and coarser sediments 
that constitute the greater part of the coastal ranges of the region. 

SULPHUR SPRING NEAR SULPHUR CREEK (SONOMA 3). 

A small cool sulphur spring which is about 3 miles northeast of 
Cloverdale, on the road to The Geysers (Sonoma 4, p. 83), rises in the 
bottom of a ravine tributary to Sulphur Creek and a few yards 
above the road. The spring has not been improved and is some- 
times covered by landsHde material, but when open it yields moder- 
ately sulphureted water and forms a roadside drinking spring. 

The rocks of the locahty consist of serpentine and of dark altered 
sandstone which probably belongs to the Franciscan formation. 
The spring apparently issues from crevices in a crushed zone in the 
sandstone. 

SULPHUR SPRINGS ON BRANCH OF DEEP CREEK (MENDOCINO 12). 

Mildly sulphureted water issues from several vents in the bed and 
along the bank of a branch of Deep Creek, on the eastern side of 
WiUits Valley about 4 miles east of Willits. The yield is apparently 



SULPHUR SPRINGS. 259 

slight, but small amounts of white algous growths on the banks and 
strings of bubbles that rise in the creek make the locality easily 
noticeable. Sandstone and shale that dip about 10° N. are exposed 
at this place. 

MUm SPRINGS (MENDOCINO 11). 

On the edge of the valley about 4 miles northeast of WiUits natural 
gas and a small flow of water have been obtained on the property of 
Mr. A. J. Muir. A collecting tank covers a small pit in which gas 
rises and is used for heating and lighting the residence a few hundred 
yards away, and a natural spring rises near by that yields about 5 
gallons a minute of mildly sulphureted water with a shght oily 
taste. A well was drilled 150 feet deep, close to the gas tank, in search 
of oil or a greater supply of gas, but obtained only a flow of cool water. 

This part of the valley is underlain by dark shales from which 
natural gas is said to escape at several other places along the eastern 
side of the meadow land. 

SULPHUR SPRING NEAR LAYTONVILLE (MENDOCINO 4). 

A spring that yields about 200 gallons a minute rises near the 
barnyard of Mr. Samuel Pinches, half a mile north of Laytonville. 
The water issues on a gentle slope at the base of a steeper hillside, 
from several vents in a small depression. It is locally called a sul- 
phur spring, and a small amount of the algous growth that is common 
in sulphur springs grows along the outflow channel, but the water is 
only faintly sulphureted. It has a distinctly minerahzed taste as of 
sulphates, however, and inflammable gas rises with the water. A 
small bathhouse is supphed by the spring, but little other use has 
been made of the water. The rock from which it rises appears to be 
a crushed quartzitic sandstone, and the topography suggests that 
the spring rises along a slight fault. 

SULPHUR SPRING NEAR BRANCH OF EEL RIVER (MENDOCINO 3). 

A small spring of distinctly sulphureted water rises in the barn- 
yard of Mr. Mitchell's ranch, on the southern side of a branch of 
South Fork of Eel River, about 13 miles by road and trail northwest 
of Laytonville and 1 mile northwest of Petersons Mineral Spring 
(Mendocino 2, p. 177). The spring has not been used for drinking or 
for other purposes, but it is of interest from the fact that its water 
was rendered milky by clay for a week following the earthquake of 
April 18, 1906. It issues in a marshy patch near the base of dark- 
colored sedimentary rocks. 



260 SPEINGS OF CALIFOKNIA. 

STJLPHUR SPRINGS NEAR CUMMINGS (MENDOCINO 1), 

Near Cummings post office, on the stage road 30 miles northward 
from Sherwood, are two sulphur springs which have not been im- 
proved but which yield flows of about 5 and 10 gallons a minute 
of cool, mildly sulphureted water that is used to some extent for 
drinking. 

SULPHUR SPRING NEAR HOAGLIN (TRINITY 4). 

Near Hoaglin post office, in the southern part of Trinity County, 
there is a spring which yields inflammable gas. The water is mildly 
sulphureted and has formed a watering place for cattle, but otherwise 
the spring has been little used. 

A few other sulphur springs issue in the rugged slopes of western 
Trinity County, but they have not been improved and are known 
to only a few residents. One such spring that has a considerable 
flow is said to issue on the side of South Fork Mountains a number 
of miles southwest of Weaverville, and others are reported at Wild- 
wood and at Coxs Bar. 

SULPHUR SPRING IN EUREKA. (HUMBOLDT 1). 

A spring of moderately sulphureted water is situated at the foot 
of H Street, in the city of Eureka. It has been known for a long 
time, but in 1910 its water had not been used for two or three years. 
The spring is about 50 feet from the shore of Humboldt Bay, and 
when examined the water stood 5^ feet below the surface, in an iron 
pipe 2 feet in diameter, within a shallow, board-curbed pit. This is 
possibly the spring mentioned by Anderson,^ who gives an analysis 
showing that the water is a strong brine, containing 30,815 parts per 
million of solids in solution and that it is saturated with hydrogen 
sulphide. 

Another sulphureted water at -Eureka, which is obtained from the 
Humboldt artesian mineral well, is mentioned among the saline 
mineral waters. 

MOUNTAIN VIEW SPRING (HUMBOLDT 3). 

Mountain View Spring is at a small resort on Mad River, about 28 
miles by road southeast of Eureka. In 1910 a hotel of 10 rooms 
and a small cottage afforded accommodations for 15 or 20 people. 
A small spring of strongly sulphureted water issues on the hillside 
600 yards west of the hotel, near a creek that is tributary to 
Mad River. Its water has been used occasionally by some ailing 
guest, but otherwise little attention has been given to the spring. 

Unaltered sandstone is exposed for about 10 miles along the 
road eastward from Eureka toward Mountain View Spring. A schist, 

1 Anderson, Winslow, Mineral springs and health resorts of Californiaj p. 133, 1892. 



SULPHUR SPRINGS. 261 

most of which contains glaiicophane, then appears as the road is 
followed southeastward up a stoop grade nearly to Kneeland post 
office, which is about 20 miles from Eureka. Chert is exposed at this 
place and extends, interspersed with a few areas of serpentine, 
southeastward nearly to Mountain View Spring. The spring 
issues in an area of andesitic lava, which is exposed on the lower 
slopes near the resort. Serpentine appears above the andesite, on the 
slopes across the creek and a short distance southeast of the spring, 
and tremolite schist was observed still higher up the hillside. 

COOK SPRING (HUMBOLDT 4). 

Cook Spring is about 7 miles south of Mountain View Spring 
(Humboldt 3, p. 160), or 35 miles by road southeast of Eureka. It is 
situated near the north bank of North Yager Creek and 10 yards 
below the road, near the point at which the road crosses the stream a 
quarter of a mile east of laqua. A pool 14 inches in diameter here 
forms a drinking basin that is used occasionally by travelers and 
by the cattle of the surrounding range. 

Several other sulphur springs of small flow issue in the upper 
portions of the basin of North Yager Creek, but they are unimproved 
and are even less important than Cook Spring. A small sulphur 
spring at Felts Springs (Humboldt 5, p. 300) is mentioned in the 
description of the saline springs at that place. 

The southern boundary of the andesite along the road from 
Mountain View Spring to Cook Spring is about 2 miles south of the 
former place. Mica schist that contains glaucophane extends from 
that point to and beyond Cook Spring and also westward along the 
road to a point about 6 miles in a direct line east of Fortuna. 
Unaltered sediments extend from this point northwestward to the 
coast. In the schist there are lenses of limestone, and many small 
sink holes have been formed by the partial solution and removal of 
this material. 

DEERLICK SPRINGS (TRINITY 3). 

Deerlick Springs are situated in the deep, rugged canyon of Browns 
Creek, 28 miles by road and trail south of WeavervUle. They are 
also reached by 9 miles of trail northward from the Midas mine 
in Harrison Gulch (Knob post office). They have long been known 
as Coumbs Springs and have been a local camping resort. A supply 
store was formerly conducted during the summer in a cabin that 
was built near the springs more than 20 years ago. During 1909 
the property changed hands, and the present name was adopted. 

There are five strongly sulphuroted springs on the property, aU 
on the west side of the creek. Two of them, known as the Blue 



262 SPRINGS OP CALIFORNIA. 

Sulphur and White Sulphur springs, from the tint of the water in 
their basins, rise about 8 yards apart, at the base of an earth and 
gravel bank beside the creek, yield respectively about 1 gallon and 
4 gallons a minute, and have deposited small amounts of sulphur 
along their overflow channels. 

About 225 yards downstream from the Blue Sulphur and White 
Sulphur springs two other strongly sulphureted springs issue from 
crevices in a light-colored siliceous rock that seems to form a ledge 
about 50 feet wide, which trends northeastward and crosses the creek 
at a small angle. One of these springs is the most important of the 
group and yields about half a gallon a minute of clear cold water that 
has a pronounced greenish-yellow tint and tastes strongly of hydro- 
gen sulphide. The other spring, 3 or 4 yards farther north, yields 
perhaps 1 gallon a mmute of water that is also strongly sulphureted 
but is colorless. The mixed water of the two springs, named Nipicuro 
by the new owner but formerly known as Deadshot, has been con- 
ducted by a small trough into a wooden tank and heated in tubs for 
bathing. During 1909 small amounts were bottled and used experi- 
mentally in the treatment of diseases of the blood, preparatory to 
putting it on the market as a medicinal water. 

Mr. F. M. Eaton has suggested that the yellow color of the principal 
spring may be due to the presence of polysulphides, and it seems 
probable that they are alkaline sulphides like those that have been 
determined in the waters of Blue Lick Springs, Ky.^ The following 
analyses of the waters have been made. The sample of Nipicuro 
analyzed by Mr. Dinsmore was collected from the tank into which 
both springs discharge and during the summer, when there was 
probably very little dilution by surface water. The sample analyzed 
by Mr. Eaton was collected from the first-described spring of the two 
forming Nipicuro, in November, during a stormy period, but at a time 
when the ground was partly frozen, so that there was little surface 
water in evidence. The difference shown by these two analyses is 
not greater than would be expected in such highly mineralized water, 
considering the different proportions of surface water that may have 
diluted the springs, and especially the fact that they were not col- 
lected at the same point. It seems probable that the carbonate 
reported in the three Dinsmore analyses represents alkalinity due to 
sulphide as well as carbonate. All of the analyses indicate secondary 
saline waters with differing proportions of primary salinity and 
secondary alkalinity. The differences in concentration are consider- 
able. 

I Matson, G. C, Water resources of the blue-grass region, Kentucky, with a chapter on the quality of 
the waters by Chase Palmer: U. S. Geol. Survey Water-Supply Paper 233, p. 209, 1909. 



SULPHUR SPRINGS. 



263 



Analyses of water from Deerlick Springs, Trinity County, Cal. 
[Constituents are in parts per million.] 



Temperature 

Pro])erlies of reaction: 

Primary salinity 

Secondary salinity. . 

Tertiary salinity 

Primary alkalinity. . 
Secondary alkalinity 
Tertiary alkalinity . . 



10°C.(50°F.) 

41 

51 







Constituents. 



By 

weight. 



Sodium (Na) 

Potassium (K) 

Ammonium (NH^) 

Calcium (Ca) 

Magnesium (Mg) 

Iron(re) t 

Aluminum ( Al) 

Sulphate (SO4) 

Nitrate (NO3) and nitrite 

(NO2) 

Chloride(Cl) 

Bromide (Br) 

Iodide (I) 

Sulphide (S) 

Carbonate (CO3) 

Metaborate(B02) 

Arsenate ( ASO4) 

Silica (Si02) 



1, 118 

28 



1,419 
11 

} ^- 

1,067 



3, 141 


159 
25 
Tr. 

11 



6, 9S4. 1 



Carbon dioxide (CO2) 

Hydrogen sulphide (H2S) 



86 



React- 
ing 
values 



By 
weight. 



48.60 
.71 



70.79 
.93 

.18 

22.23 



Tr. 
}l,520 



88.64 
.00 
.00 
9.34 
.82 
Tr. 
.00 
.37 




3,750 



a9,480 



398 



React- 
ing 

values. 



By- 
weight. 



1,332 
163 



Tr. 

75.90 



f 1,622 
I 21 

9.5 
1,504 



.00 
105.80 



3,463 
5.2 



268 
Tr. 



8,312.7 



23.37 




118 



React 

ing- 

values, 



By 
weight. 



57.90 
4.17 



50 
8.2 



75.95 
1.76 

.34 

31.33 



108 
11 

0.3 

94 



97.70 
"".Oi 



184 



8.94 
Tr. 



36 





6.91 



(6) 
Trace. 



mg 
values, 



By 
weight. 



React- 
ing 
values- 



2.18 
.21 



47 
5.7 



5.38 
.93 

.01 

1.95 



132 

12 

2.0 
85 



5.19 



262 



1.56 



19.8 



1.18 



597.5 



(6) 
Trace. 



2.05 
.15 



6.62 
.99 

.07 

1.77 



(6) 
(.0) 



a Total solids. 



6 Present. 



1. Nipicuro Spring. Analyst and authority, F. M. Eaton (1909). Sample from spring having the 
greater flow. 

2. Nipicuro Spring. Analyst, T. W. Melia (1911). Authority, owner of springs. Taken from a sani- 
tary analysis of water bottled direct from spring. 

3. Nipicuro Spring. Analyst, S. C. Dinsmore (1909). Authority, owner of springs. Sample bottled 
after standing. 

4. Blue Sulphur Spring. Analyst, S. C. Dinsmore (1909?). Authority, owner of springs. 

5. White Sulphur Spring. Analyst, S. C. Dinsmore (1909?). Authority, owixer of springs. 

A fifth spring, known as the Highshot Spring, issues on the side of a 
ravine about 125 yards northwest of the Nipicuro Spring and about 
the same distance from the creek. Like the others, it is strongly 
sulphureted and of slight flow, but it has been comparatively little 
used. 

The rocks of the region consist of the series of altered sediments 
and of serpentine that forms the greater part of the northern Coast 
Ranges. Near the springs there is considerable impure limestone or 
calcitic sandstone, which probably accounts for the large amount of 
calcium in the spring water. Quartz porphyry was observed on the 
mountain ridge a mile south of the spring, and float of the same 
material was found along the creek. 



264 spehstgs of califoenia. 

sulphur springs on browns creek (trinity 2). 

Sulphur water issues at several places along the course of Browns 
Creek, notably at points about four-fifths mile, li miles, and 1| miles 
below Deerlick Springs (Trinity 3, p. 261), appearing in places on the 
western bank of the creek and also in its bed. These lower springs 
have not been improved, but they are near the trail and are noticeable 
because of the sulphur-coated algous growths along their run-off 
channels. On the eastern side of the creek, nearly opposite the spring 
farthest downstream, a strongly sulphureted spring that yields 
perhaps 1 gallon a minute, issues from crevices in a dark, schistose 
rock beside the trail. Bubbles of inflammable gas that is probably 
hydrogen sulphide rise in the small pool that is formed in a natural 
basin in the rock. These springs are doubtless similar in origin and 
character to Deerlick Springs. 

NEYS SPRINGS (SISKIYOU 18). 

The sulphur springs that have thus far been described are on the 
western slopes of the northern Coast Ranges. There are also a few 
sulphur springs on the eastern slopes that are drained by tributaries 
of Sacramento River. The northernmost of these springs that are 
worthy of note are Neys Springs, in the canyon of Little Castle Lake 
Creek, 5 miles southwest of Sisson. They were discovered in 1887 
by Mr. John Ney, who has improved them and established a small 
resort for the medicinal use of the waters. At this place there are 
three mineralized springs, the two less important being sulphureted 
and the principal one of less usual character. 

The principal spring rises at the northern side of the creek and was 
formerly submerged during periods of high water. It has been pro- 
tected by rockwork and the channel has been filled in, however, so as 
to form a pool about 7 feet in diameter a few feet from the creek edge. 
The outflow (Aqua de Ney) is piped to a tank and heated for use in a 
bathhouse near by. Bubbles constantly rise in the pool, in which the 
water is clear but slightly amber in tint. It is a water of very unusual 
character, inasmuch as it smells and tastes strongly of ammonia and 
appears to have caustic alkalinity. This fact was commented on by 
the analyst, who states that after making a number of confirmatory 
tests he is unable to account for the alkalinity in any other way than 
by assuming the presence of the hydroxide radicle. It is not unlikely 
that a part of the alkalinity is due to silicate." 

The water apparently rises from a seam of claylike decayed ser- 
pentine, a few inches wide, in a dark schistose rock that is exposed for 
a number of yards along the bed and sides of the creek. It has been 
suggested by Mr. Eaton that the remarkable ammoniacal character 
of the water may result from the action of ferrous iron derived from 



SULPHUR SPRINGS. 



265 



the docayed serpentine on nitrates derived from buried organic 
material. 

About 75 yards eastward downstream a cold, mildly sulphureted 
spring, called Milton Spring, issues from a crevice in a ledge of the 
schist on the opposite side of the creek and several feet above it. 
Water from this spring has been used for drinking. A few yards 
farther north there is a small seepage pool of sulphureted ammoniacal 
water, which has been used only slightly for drinking and for sham- 
pooing. The following analyses represent water from the two 
principal springs: 

Analyses of water frovfi Neys Springs, Siskiyou County, Cal. 
[Analyst and authority, F. M. Eaton (1910). Constituents are in parts per million.] 



Aqua de Ney. 



Milton Spring. 



Properties of reaction: 

Primary salinity 

Secondary salinity. . . 

Tertiary salinity 

Primary allcaliriity . . . 
Secondary alkalinity. 
Tertiary alkalinity. . . 



43 


57 
Trace. 
3 



Constituents. 



Sodium (Na) 

Potassium (K) 

Ammonium (NHi). 

Calcium (Ca) 

Magnesium (Mg)... 

Iron(Fe) 

Aluminum (Al) 

Sulphate (SO4) 

Chloride (01) 

Hydroxide (OH)... 

Sulphide (S) 

Carbonate (CO-,)--. 
Metaborate (BO2). . 
Phosphate (PO4)... 
Silica (SiOa) 



Carbon dioxide (CO2) 

Hydrogen sulphide (H2S). 



By 
weight. 


Reacting 
values. 


By 
weight. 


Reacting 
values. 


11,090 

72 
152 


482.4 
1.8 
8.4 

Trace. 
.6 

Trace. 

5.7 
206.2 
101.1 

16.5 
162.4 
Trace. 
Trace. 

13.9 


151 
8.9 


6.57 
.23 


Trace. 
7.2 

!• Trace. 

272 
7,310 
1,720 
264 
4,872 
Trace. 
Trace. 
420 


20 
5.5 

1.7 

18 
51 


1.00 

.45 

.06 

.37 
1.44 






139 


4.64 






92 


.3.05 


26,179.2 




487.1 









.00 



Present. 
Present. 



Present. 
Present. 



Both Springs are essentially primary alkaline and saline in character. 
The deficiency in acid radicles commonly found in water is especially 
noteworthy. The water of the Milton Spring, though differing in 
several particulars from that of the main spring, appears to have 
the same origin. It is a water such as would be produced by diluting 
water from the main spring with surface water. 

There are benches of gravel along the canyon sides for half a mile or 
more above and below the springs. Farther down the canyon some 
gabbroid rock was noticed, but nearly to Cantara raiboad station, 2 
miles away, the canyon walls are mainly of light-colored lava, 
probably andesitic, which at one place forms prominent cliffs. 



266 SPRINGS OF CALIFORNIA. 

SULPHUR SPRING ON CASTLE CREEK (SHASTA 1). 

A small sulphui' spring issues in the canyon of Castle Creek about 
4 miles west of Castella railroad station. The spring is not easily 
accessible, however, as it is in a steep and brushy region and has not 
been improved nor often visited. In connection with its occurrence, 
a small, faintly sulphureted spring (Shasta 5) may be mentioned, 
which issues at the edge of Sacramento River near the mouth of 
Castle Creek. This latter spring is more noticeably carbonated, 
however, so it has been described with the carbonated springs (p. 227). 
The water of Castle Rock Springs (Shasta 4, p. 226), which are at the 
edge of Sacramento River about one-half mile above the mouth of 
Castle Creek, is also sUghtly sulphureted as well as carbonated in 
character. 

COLYEAR SPRINGS (TEHAMA 10). 

Colyear Springs are situated high on the mountain side, 35 miles by 
road westward from Red Bluff. Six springs here rise in basins in a 
cemented place about 5 yards in diameter, among the pine trees on a 
moderate slope. All yield flows of cool water varying in amount 
from mere seepages to about 2 gallons a minute. One of the largest 
is noticeably sulphm-eted, but the others are only faintly so. On the 
slopes about 8 yards above them there is a clear-water spring that 
yields 4 or 5 gallons a minute. 

An attempt was early made to estabUsh a resort at Colyear Springs, 
but it met with little success. Within recent years, however, several 
cabins have been built, a road of easier grade has been constructed up 
the mountain, and the place has been used to some extent as a 
mountain resort. 

HENSLEY SPRING (TEHAMA 9). 

Hensley Spring is about 4 miles by trail west of north from Colyear 
Springs and about 450 feet lower down the mountain side. It rises 
at the edge of a clump of black oaks, on a low ridge betv/een two 
ravines, in an area that is covered with dense brush. It furnishes 
sufficient water for plant growth, forming a small green patch within 
which there are a few wiUow trees. The spring rises partly as seepage 
and partly from a shallow basin in the soil. Its water is noticeably 
sulphureted and deposits a small amount of iron. The spring has 
long been known, but the place has been abandoned since the early 
nineties, and a cabin that stood near the spring was destroyed by a 
brush fire several years ago. A much smaller spring, similar in 
character to Hensley Spring, issues in the bed of a ravine a mile 
southward. 



SULPHUR SPRINGS. 267 

Dark shales that dip steeply eastward are well exposed in the 
ravines and canyons of the lower slopes of this region.^ Near both 
the Colyear and Hensley springs, however, the rocks are altered, and 
schists were observed associated with siliceous sediments veined with 
quartz. Serpentine is exposed for most of the distance between the 
locahties of the two springs and apparently forms a dike that trends 
west of north across the slopes. 

SULPHUR SPRING ON SOUTH FORK OF COTTONWOOD CREEK 

(TEHAMA 8). 

There is a sulphiu* spring in the canyon of South Fork of Cotton- 
wood Creek, about 4 miles west of Toms Head Mountains and 10 miles 
in a direct line northwest of Colyear Springs, but it is in a brushy 
region, is difhcult of access, and has been seldom visited. The rocks 
in the vicinity are the sedimentary and metamorphic rocks of the 
Coast Ranges, such as were noted at Colyear Springs and Hensley 
Spring. 

SULPHUR SPRING SOUTHWEST OF FOUTS SPRINGS (COLUSA 2). 

A spring about 1 mile by trail south and west of Fouts Springs 
(Colusa 3, p. 205), in the upper end of a Uttle glade on the brushy 
slopes, forms a small pool, from which there is a flow of about 5 
gallons a minute of water that tastes mildly sulphureted and sHghtly 
salty. A deposit of Ume carbonate that crusts the surface for sev- 
eral yards below the spring indicates that the water also contains 
calcium and carbon dioxide in considerable amounts. The spring 
has been occasionally visited by guests from Fouts Springs, but it 
has not been permanently improved as a drinldng spring. 

SULPHUR SPRING WEST OF FOUTS SPRINGS (COLUSA 1). 

A sulphur spring that is similar in character and mode of occur- 
rence to that southwest of Fouts Springs (Colusa 3) issues on "Old 
Joe's" place, about H miles west of Fouts Springs. It yields perhaps 
10 gallons a minute of mildly sulphureted water and was formerly 
used in irrigating a garden. Durmg recent years, however, it has 
been unused, and as it lies on a steep mountain side it has been 
seldom visited. 

The rocks near both of the sulphur springs described in the fore- 
going paragraphs consist of the series of altered sediments and asso- 
ciated serpentine that is common in this region. The springs 
apparently issue from altered sandstone. 

1 These deposits have been described by J. S. Diller (Tertiary revolution in the topography of the 
laciflc coast: U. S. Geol. Survey Fourteenth Ann. Kept., pt. 2, p. 406, 1894). 



268 SPRINGS OF CALIFORISriA. 

SULPHUR SPRING NEAR BLUE LAKES (LAKE 17). 

A small flow of mildly sulphureted water issues in a ravine one- 
third of a mile south of Blue Lakes resort, which is 19 miles by road 
north of east from Ukiah. The water emerges at the base of a bank 
of gray sandstone into a cemented drinking pool. It was at one time 
piped down the ravine to the resort, but in 1909 it was apparently 
used only at the spring. A partial analysis of the water, published 
in advertising matter, shows it to be mildly mineralized, with sodium 
and sulphate predominating. 

HAYVILLA SULPHUR SPRING (LAKE 16). 

In an open drainage course 5 miles northwest of the town of Upper 
Lake there is a sulphur spring whose water has been used to some 
extent for bathing and drinking. It has become known as Hayvilla 
Sulphur Spring, from the name of the ranch on which it is situated. 
When the place was visited the water rose from buff-colored sand- 
stone near the drainage wash into a small rock-walled drinking pool, 
and was piped to a bathtub a few yards away. The water is notice- 
ably sulphureted and has a slightly alkaline or saline taste. 

In connection with the Hayvilla Spring, two other sulphur springs 
in the same region, which have already been described, may be men- 
tioned here. One of these is about 3 miles westward, on the property 
of the Witter Medical Springs Co. (p. 177); the other is at Saratoga 
Springs (Lake 18, p. 179), about 3 miles southward in a direct line. 

SULPHUR SPRINGS IN SULPHUR VALLEY (LAKE 43). 

Two small unimproved springs that are noticeably sulphureted 
lie in Sulphur Valley, in southern Lake County, 2 or 3 miles north- 
east of Glenbrook post office. One of these springs is on the Ogden 
ranch, and rises near a small spring of distinctly carbonated water; 
the other, which is some distance westward and is known locally as 
the Deadshot Spring, is alkaline and saline, as well as sulphureted, 
and its water is said to have been used for curing deer hides by putting 
them to soak in the spring. 

ZEM ZEM SPRING (NAPA 1). 

A small spring of strongly sulphureted water is situated near the 
road between Knoxville and Monticello, about 5 miles southeast of 
Knoxville. The spring was of more importance during the days of 
active mining in the Knoxville district than it is now, but it is still a 
camping place for teamsters. The water is too highly mineralized, 
however, to be palatable, an early analysis ^ indicating a content of 
21,000 parts per million of total solids. 

1 Crook, J. K., The mineral waters of the United States and their therapeutic uses, p. 176, 1899. 



SULPHUR SPRINGS. 



269 



PIEDMONT SPRINGS (ALAMEDA 1). 

Piedmont Springs are in a recreation park on the hillside 3 miles 
north of Oakland. 

Two mineralized springs, which are laiown, respectively, as Sulphur 
and Magnesia springs, rise in a ravine that extends through the prop- 
erty. The springs have been curbed and covered, and the ravine has 
been graded for a walk. The waters are piped about 100 yards 
downstream into two drinking basins in a grotto-like spring house 
that is built against a rock face at the side of the ravine. A third 
basin in the spring house is supphed from the municipal water main. 
The water of both springs is noticeably sulphureted, and that of the 
Magnesia Spring also tastes distinctly alkahne. The following 
analyses show the characters of the waters. Both have noteworthy 
primary salinity and secondary alkalinity, but although the sulphur 
spring is characterized by secondary salinity, the magnesia spring 
has high primary salinity. 

Analyses of luater from Piedmont Springs, Alameda County, Cat. 
[Analyst and authority, Winslow Anderson (1889). Constituents are in parts per million.] 



Sulphur Spring. Magnesia Spring. 



Temperature 

Properties of reaction; 

Primary salinity 

Secondary salinity. . . 

Tertiary salinity 

Primary alkalinity. . . 

Secondary alkalinity. 

Tertiary alkalinity. . . 



1G° C. (60° F.) 

42 
15 


43 
29 



14° C. (58° F.) 

23 


36 
41 



Constituents. 



Sodium (Na) 

Potassium (K) 

Calcium (Ca) 

Magnesium (Mg) . . . 

Iron (Fe) 

Aluminum (Al) 

Sulphate (SO4) 

Chloride (CI) 

Iodide (I) 

Carbonate (CO3).... 
Metaborate (BO2)" 
Silica (Si02) 6 



Carbon dioxide (CO2) 

Hydrogen sulphide (II2S}. 



weight. 



151 

7.4 

58 

77 

Trace. 

Trace. 

329 

■ 82 

Trace. 

196 

14 

87 



1,001.4 



Reacting 
values. 



By 

weight. 



6.55 
.19 

2.92 

6.35 
Trace. 
Trace. 

6.84 

2.32 
Trace. 

6.53 
.32 

2.87 



113 

31 

23 

35 

14 
4.1 

33 

53 

Trace. 

215 

38 

72 



631.1 



1.78 
3.58 



62 
Trace. 



Reacting 
values. 



4.93 
.78 

1.13 

2.88 
.51 
.45 
.69 

1.49 
Trace. 

7.16 
.89 

2.38 



2.80 
Trace. 



a Reported as "borates;" recalculated from Na2B407. 
b Reported as "silicates;" assumed to be Si02. 

The second analysis is given by Anderson' as from an "iron 
spring," but this is believed to be the same spring that is now known 
as the Magnesia Spring. 



Anderson, Winslow, Mineral springs and health resorts of California, p. 223, 1892. 



270 SPKIJSTGS OF CALIFORNIA. 

Sandstone associated with serpentine exposed near the springs 
probably belongs to the Franciscan formation of old sediments and 
metamorphic rocks, which occupies considerable areas in the central 
portion of the coastal region. 

SULPHUR SPRINGS NEAR WALNUT CREEK (CONTRA COSTA 3). 

A group of sulphur springs lies near the northeastern base of a 
low ridge about 2 miles northeast of the town of Walnut Creek. The 
largest spring is on the ridge, about 100 yards from its eastern base 
and 25 yards north of the county road. When the place was visited, 
the water rose in a board-curbed pool protected by a latticed house 
and was piped to a cattle trough a few yards away. It yielded about 
3 gallons a minute of mildly sulphureted water, 81° in temperature. 
On account of this noticeably high temperature the springs are indi- 
cated on Plate III (in pocket) as thermal sulphureted. Five other 
smaller sulphur springs issue in a belt extending 350 yards along 
the base of the ridge, in and near the barnyard of Sulphur Springs 
farm. Two of them have been piped to watering troughs near by. 
The other three are of seeping flow and form only small marshy 
places. 

The ridge is composed of sandstone that appears to dip nearly 
vertically and strike S. 30° E. (magnetic) along the trend of the 
ridge. The steep inclination of the beds shows that intense move- 
ment has taken place here, and a fault that is indicated on Plate III 
extends along the border of the valley land. This structural break 
probably accounts for the rise of the springs and also for their thermal 
character. 

SULPHUR SPRING IN PINE CANYON (CONTRA COSTA 4). 

A moderately sulphureted spring emerges about 4 miles m a 
direct line northward from Danville, in Pine Canyon, which is at 
the western base of Mount Diablo. The water forms a clear pool, 
about 15 inches wide and 4 feet long, in thick-bedded sandstone at 
the southern side of the creek. The yield is larger than is usual for 
springs of this class, being estimated at 5 gallons a minute, and the 
temperature of the water (67°) is also somewhat above the normal. 
The spring has not been improved, but it has been visited by occa- 
sional picnic parties. There are three seepages within 5 yards of 
the spring, and 1^ miles farther eastward, upstream, sulphureted 
water seeps from a bluff on the northern side of the creek. Only the 
one spring of appreciable flow was observed along the canyon, 
however. 

MAYHEW SPRING (ALAMEDA 2). 

Mayhew Spring is about 200 yards north of Niles depot. It is 
situated in an orange orchard and is surrounded by a cemented stone 
curbmo; which forms a reservoir about 4 feet in diameter and 10 feet 



SULPHUR SPRINGS. 271 

deep. A small pipe and faucet furnish an outlet from a point about 
3 feet below the surface, but the yield is only about 1 gallon a minute 
of water that had an observed temperature of 67° in the reservoir. 

The spring was loiown to the Spaniards in the early days and is 
still used to slight extent for drinking. Bubbles of gas continually 
rise in the reservoir, but the water is only faintly sulphureted. The 
spring is situated on a gentle alluvial slope at the mouth of a drainage 
wash, between hills of sedimentary rocks that are probably of Tertiary 
age. 

In connection with the Mayhew Spring, Warm Springs (Alameda 
3, p. SO), which have been described among the hot springs, may be 
mentioned, as they are along the same range of hills although about 6 
miles southeastward. They are also famtly sulphureted but are 
named and best known as Warm Springs. There are other sulphur 
springs, described already (see p. 208), in Alum Rock Park, about 
18 miles southeast of Mayhew Spring. At these three localities the 
warm sulphur water emerges along the front of hilly slopes where a 
fault has been traced, and the springs seem therefore to be closely 
related to this structural break. 

SULPHUR SPRING ON CROW CREEK 'STANISLAUS 1). 

A few sulphur springs of small flow issue along the stream channels 
on the northeastern border of San Joaquin Valley. One of these is 
situated on Crow Creek, about 10 miles west of Newman, but it has 
not been developed and is of little importance. 

SULPHUR SPRINGS ON ORESTIMBA CREEK (STANISLAUS 2). 

About 8 miles southwest of the sulphur spring on Crow Creek 
(Stanislaus 1) two other sulphur springs that have only a shght flow 
issue from the banks of Orestimba Creek. Like the one farther 
northeast, they have not been used and are unimportant. 

The rocks that border this portion of San Joaquin Valley consist 
of gravels and finer sediments, probably of Tertiary age. 

HILLYDALE SULPHUR SPRING (SANTA CLARA 6). 

A small sulphur spring is situated on property known as Hillydale, 
about 4 J miles south of the reduction works of the New Almaden 
quicksilver mine, or 20 miles by road southward from San Jose. 
The spring is on the western bank of a stream, 200 3'^ards from the 
house on the place, and yields about one-half gallon a minute of 
moderately sulphureted water. The following analysis indicates a 
primary-saline, secondary-alkahne water whose total mineral content 
is small. 



272 



SPRINGS OF CALIFORNIA. 



Analysis of luater from Hillydale Sulphur Spring, Santa Clara County, Cal. 
[Analyst, F. T. Green (1904). Authority, owner of spring. Constituents are in parts per million.] 



Properties of reaction: 

Primary saliaity 

Secondary saliaity 

Tertiary saliaity 

Primary alkaliaity 

Secondary alkaliaity 

Tertiary alkaliaity 

Constituents 

Sodium (Na) 

Calcium (Ca) 

Magnesium (Mg) 

Iron(Fe) 

Alumiaum ( Al) 

Sulphate (SO^) 

Chloride (CI) 

Carboaate (CO3) 

SiUca (Si02) 

Hydrogen sulphide (H2S) 



By 
weight. 



Reactiag 
values. 



95 
32 
9.5 



39 
104 
83 
11 



4.12 
1.60 

.78 

.04 

.81 
2.93 
2.76 

.37 



Present. 



Present. 



The water is used locally for drinking and is considered useful 
medicinally. 

The spring is situated at the base of a basaltic slope, in an area 
of sedimentary rocks that may belong to the Franciscan formation. 
The rock near the spring contains much calcite and is stained with 
metallic sulphides, from which the sulphide constituents of the water 
are possibly derived. 

HINNS SULPHTJB, SPRING (SANTA CRUZ 2). 

About 4 miles south of Hillydale Sulphur Spring, across a mountain 
divide, is a small spring known as Hinns Sulphur Spring, It has 
been used to some extent for drinking, but has not been greatly 
improved and has only local interest. 

OLIVE SPRING (SANTA CRUZ 1). 

Olive Spring is about 1 mile west of Hinns Sulphur Spring. Like 
the latter it has been of only local importance, as it yields but a smaU 
flow of moderately sulphureted water and is remote from well- 
traveled roads. 

Analyses of "Nicholas Springs," pubhshed by Anderson, are 
probably of water from either Ohve or Hinns springs. They show a 
solid content of about 3,100 parts per million, with calcium, mag- 
nesium, and sulphate as the prominent constituents. 

SULPHUR SPRING ON BODFISH CREEK (SANTA CLARA 11). 

Several mineralized springs issue along Bodfish Creek and its 
tributaries west of Gdroy. Not all of these springs are sulphureted, 
but as hydrogen sulphide is the most prominent constituent of some 
of them, the group is described among the sulphur springs. 



SULPHUR SPRINGS. 273 

A strongly siilphureted spring is situated on the northern bank of 
Bodfish Creek, about 7 miles west of Gilroy and 75 yards above the 
pomt where the wagon road crosses the stream and both road and 
stream make a sharp bend from an easterly to a northerly direction. 
The water issues in a pool about 1 by 3 feet across that has been dug 
in the bank 5 yards from the stream. The pool is usually covered 
with a scum of sulphur and there is a strong odor of hydrogen sul- 
phide near it. The water is used to a slight extent for drinking by 
campers and teamsters. 

BLODGETT MAGIC SPRING (SANTA CLARA 12 1. 

About a quarter of a mile below the sulphur spring on Bodfish 
Creek (Santa Clara 11, p. 272) there is a spring that has been known 
as Blodgett Magic Spring and visited by campers during many sum- 
mers. The water issues in a board-curbed and inclosed pool near camp 
grounds, at the base of the canyon side 25 yards east of the stream. 
It is not strongly mineraUzed, but tastes slightly saline and is mildly 
sulphureted and carbonated. The second of the two analyses on 
page 274 is thought to represent water from this spring. The analysis 
shows a primary and secondary alkaline water with notable tertiary 
alkalinity and primary salinity. In former years it was bottled and 
sold locally to small extent. The water issues from soft white 
sandstones. 

Other noticeably sulphureted and carbonated seepages issue along 
the course of the stream at short distances above and below this 
spring, and there is said to be a more distinctly carbonated spring 
several miles southeastward. 

BLODGETT MINERAL SPRING (SANTA CLARA 10). 

A spring that is known as the Blodgett Mineral Spring or Magnesia 
Spring is situated on the hillside above a branch of Bodfish Creek and 
several miles north of Blodgett Magic Spring. It issues from ser- 
pentine and its water is piped from a small covered and rock-waUed 
basin 1 mile eastward to a tank near a farm house. The follo\ving 
analysis of the water shows that besides containing a large proportion 
of magnesia, the water of Mineral Spring is primary and secondary 
sahne in character. 

35657°— wsp 338—15 18 



274 



SPRINGS OF CALIFOENIA. 



Analyses of water from Blodgett Mineral Spring and Blodgett Magic Spring, Santa 

Clara County, Cal. 

[Analyst and authority, Winslow Anderson (1889). Constituents are in parts per million.] 



Mineral. 



Magic. 



Properties of reaction: 

Primary salinity 

Secondary salinity 

Tertiary salinity 

Primary alkalinity 

Secondary alkalinity 

Tertiary alkalinity 

Constituents 

Sodium (Na) 

Potassium (K) 

Calcium (Ca) 

Magnesium (Mg) 

Iron (Fe) 

Aluminum (Al) 

Sulphate (SO4) 

Chloride (CI) 

Iodide (I) 

Carbonate (CO3) 

Metaborate (BO2) 

Silica (Si02) 

Carbon dioxide (CO2) 

Hydrogen sulphide (H2S) 



By 
weight. 



Reacting 
values. 



By 
weight. 



Reacting 
values. 



Ill 

34 

30 

68 

Trace. 

Trace. 

222 

112 

Trace. 

151 

Trace. 

93 



4.83 
.88 

1.48 

5.62 
Trace. 
Trace. 

4.63 

3.15 
Trace. 

5.03 
Trace. 

3.08 



129 
4.7 
61 
37 
Trace. 
37 
42 
85 



5.61 
.12 

3.05 

3.03 
Trace. 

4.15 
.88 

2.40 



256 

Trace. 

70 



8.53 

Trace. 

2.33 



821 



32 



1.45 
2.81 



79 
Trace. 



3.58 
Trace. 



EL PAJARO SPRINGS (SANTA CRUZ 3). 

El Pajaro Springs are situated near the northern bank of Pajaro 
River and about a quarter of a mile eastward upstream from the 
Southern Pacific Railroad bridge near Chittenden station. At least 
12 cool, strongly sulphureted springs issue at this place along a 
sloping bank about 20 feet high that borders a flat willow-grown 
area along the river. The springs rise at intervals of a few yards for a 
distance of about 120 yards along the bank, being 25 to 50 yards from 
the edge of the river during normal stages of the water. Three of 
the springs, each of which yields 1 or 2 gallons a minute, have been 
used locally for many years for drinking. One of these has been 
known as the RaUroad Spring, as it has been a favorite with some of 
the railroad men. The other two, which are about 75 yards north- 
west of it, are known as White Sulphur Springs. The water of the 
Railroad Spring has the dark appearance that is characteristic of 
so-called black sulphur springs, but it becomes milky from suspended 
sulphur when it stands in an open vessel for a short time. The water 
of the White Sulphur Springs becomes milky and deposits native 
sulphur after flowing a few yards from the sources. The difference 
between the Black Sulphur or Railroad Spring and the White Sul- 
phur Springs is possibly due to different degrees of oxidation of the 
sulphide constituents in the water as it reaches the surface. The 
same feature is shown in several minor springs of the group. 



SULPHUR SPRINGS. 



275 



The springs were long known locally as Chittenden Sulphur Springs, 
but were not improved until 1909, when concrete basins were con- 
structed around the springs and the property opened to the public 
as Shale Sulphur Springs. Later the name was changed to El Pajaro. 

The follomng analyses of water from the Railroad Spring and the 
larger of the White Sulphur Springs show them to be secondary 
alkaline, primary saline waters: 

Analyses of water from El Pajaro Springs, Santa Cruz County, Col. 
[Constituents are in parts per million.] 



Properties of reaction: 

Primary salinity 

Secondary salinity. . . 

Tertiary salinity 

Primary alkalinity . . . 
Secondary alkalinity . 
Tertiary alkalinity. . . 



(?) 



(7) 



Constituents. 



By 
weight. 



Sodium (Na) 

Potassium (K) 

Lithium (Li) 

Barium (Ba) and strontium (Sr). 

Calcium (Ca) 

Magnesium (Mg) 

Iron(Fe) 

Aluminum (Al) 

Sulphate (SOO 

Chloride (CI) 

Sulphur (S) o 

Carbonate (CO3) 

Metaborate ( BO2) 

Phosphate (PO4) 

SiUca (Si02) 



Carbon dioxide (CO2) 

Hydrogen sulphide (HjS). 
Methane (CHO 



199 

4.3 




154 
83 

6.2 

150 
193 

.4 

402 





58 



1,249.9 



Present. 
4.8 



Reacting 
values. 



By 
weight. 



8.63 

.11 

.00 

.00 

7.66 

6.81 

.22 

3.12 
5.45 
.02 
13.41 
.00 
.00 
1.92 



159 
4.5 



182 



234 
109 

392 



57 



Present. 

.28 



Present. 

8.6 

Present. 



Reacting 
values. 



By 
weight. 



6.94 
.12 

.00 

.00 

9.08 

6.88 

.10 
4.85 
3.08 

.05 
13.07 

.00 

.00 
1.88 



Present. 

.50 

Present. 



28 



Reacting 
values. 



1.77 



1.67 



a In suspension. 

1. Railroad Spring. Analyst, Riddell and McCreary (1908). Authority, owner of springs. 

2. White Sulphur Spring. Analyst, Riddell and McCreary (1908). Authority, owner of springs. 

3. White Sulphur Spring. Analyst and authority, F. M. Eaton (1909). 

The first two samples were analyzed several weeks after they were 
collected. In order to determine, if possible, to what extent change 
had taken place in the unstable sulphur compounds between the 
times of collection and analysis, a sample from the White Sulphur 
Spring was later collected in a bottle containing iodme solution, so 
that the sulphide constituent was at once precipitated as sulphur 
according to the reaction HjS + 21 = 2HI + S and could be determined 
independently of the sulphate radicle. The sulphide and sulphate 
constituents were then determined witliin a few days of the time of 
collection, with the results shown in the analysis by F. M. Eaton, 
These results are not very satisfactory, however, for although the 



276 sPEiisrGS op califoenia. 

content of hydrogen sulphide is much greater in the sample treated 
with iodine than in the other, the much smaller amount of sulphate 
indicates that there was a marked change in the concentration of the 
water during the year that intervened between the collection of the 
two samples. However, in the first samples there appears to have 
been a considerable increase in the amount of sulphate in the water 
on standing, and a decrease in the sulphides, a change that probably 
somewhat alters the medicinal properties of the water. Although 
sulphides were not reported in the analyses, the change that takes 
place in the sulphur compounds when the water stands for a time is 
believed to show that sulphides are present. 

Considerable inflammable gas rises in several of the springs. 
Analysis ^ of a sample of this gas indicates that it consists principally 
of methane (marsh gas, CH^), with carbon dioxide (COg), and 
hydrogen sulphide (H2S) . 

A third of a mile north of El Pajaro Springs are two other springs, or 
wells. One issues at the base of a steep hillside through a 1 2-inch casing. 
A few bubbles of gas rise with the water and the surface of the pool that 
surrounds the casing is covered with a film of oil. The spring yields 
a,bout 1^ gallons a minute of sulphureted water that becomes milky 
by the time it reaches a watering trough 10 yards away. The other 
spring is situated in meadowland, 300 yards northwest of the first. 
It yields perhaps 8 gallons a minute of clear water that is not notice- 
ably sulphureted. It has been piped to a near-by storage tank for 
supplying cattle troughs. 

The rock of this area is hght-colored shale of Tertiary age. Oil is 
obtained from wells a few miles to the northeast. The fault zone 
along which the earthquake of April 18, 1906, took place passes 
through the locahty. The shale along the fault zone has been 
crushed by the earth movements, and landshdes have been caused by 
the shocks. The issuance of gas and sulphur water along this zone 
of shattered material, where escape for them has been furnished, is 
noteworthy. 

SULPHUR SPRING ON MISSION CREEK (MONTEREY 6). 

About 12 miles west of north from Jolon post ofiice, or 10 miles 
from San Antonio Mission, there is a cool sulphur spring that has been 
used to a shght extent as a drinking spring. It is not near a main 
traveled road, however, and is not widely known. The spring appar- 
ently issues from sedimentary materials, probably of Tertiary age, 
that form the hills bordering the west side of Salinas Valley. 

1 Analysts, Riddell and MeCreary, 1908. 



SULPHUR SPRINGS. 277 

HUER HUERO SPRINGS (SAN LUIS OBISPO 4). 

Two groups of mineralized springs, that are known as the Huer 
Huero Springs, rise on the ranch of the same name, 13 to 15 miles 
southeast of Paso Roblos. Tlie northernmost, which is known as the 
Old Spring, is on the eastern side of the road and about 1^ miles south 
of Creston post office. The water issues in the stream channel at the 
head of a creek, and jdelds a small flow of cool sulphureted iron water. 
The locahty is well shaded by oaks and willows and has been used as a 
summer camp ground for more than 20 years. It is the site of the 
Keunard German settlement, wliich was started a number of years 
ago. Tlie New Springs, which are across a drainage divide and about 
2 miles farther south, are locally known as iron springs, though their 
water is strongly sulphureted. They rise for a distance of about 100 
yards along a stream channel and yield about 2 gallons a minute. 
Like the Old Spring, the New Springs are used by campers. At both 
locahties the water issues from the light-colored granitic material that 
forms a considerable portion of the liills southeast of Paso Robles. 

SULPHUR SPRING IN CARRIZO PLAIN (SAN LUIS OBISPO 12). 

A number of small springs in the region between Paso Robles and 
the San Joaquin Valley are sulphureted, but few of them are of par- 
ticular interest, and very few are of greater use than as cattle-watering 
holes. One spring that is in the southern portion of Carrizo Plain 
has been developed to the extent of piping its water about a mile 
northward to a 10,000-gallon iron tank which supplies two cattle 
troughs. It yields about 3 gallons a minute of strongly sulphureted 
water. 

The hydrogen sulpliide of most of the springs- in this region is 
probably derived from sulphide minerals in the sediments of Ter- 
tiary age, which form the greater part of the hills that border the 
plains.^ 

SULPHUR SPRINGS ON BURTON MOUND (SANTA BARBARA 6). 

A number of sulphur springs of small flow formerly issued near the 
beach in Santa Barbara, from the sUght elevation known as Burton 
Mound, on which the Potter Hotel has been built. Since the construc- 
tion of the hotel, about 1901, the water of the springs has been 
pumped to a small drinking fountain in the hotel office and another 
at the southeastern border of the grounds. The springs rise in a small 
basin in the basement of the hotel. Although considerable difficulty 

1 "Bitterwater Spring" is shown on some early maps, about 15 miles northwest of the sulphur spring in 
Carrizo Plain. In 1910, however, it was not found, and information concerning it was unsuccessfully sought. 
It is probably a minor sulphureted spring near the channel of Bitterwater Creek. 



278 SPRINGS OF CALIFORNIA. 

was experienced in controlling the flow during construction of the 
hotel, the springs now yield only a slight amount of moderately 
sulphureted water. 

LYONS SPRING (VENTURA 6). 

Lyons Spring has been mentioned incidentally in speaking of 
Stingleys Hot Springs (Ventura 5, p. 63). It is situated in Matilija 
Canyon, about halfway between Vickers and Matihja hot springs, 
and about 1 mile- northwest of the latter place. The property has 
been open as a small resort since 1888, accommodations being pro- 
vided in 1908, by tent houses, for about 50 people. 

The spring rises in a ravine to the south, and the water is piped 
1,100 feet to a small stone reservoir on the gTOunds. It is thence 
piped to a boiler and heated for bathing. It is soft and mildly 
sulphureted, being known as a white-sulphur water from the shght 
milkiness that is produced by sulphur in suspension. 

SULPHUR SPRING IN MATILIJA CANYON (VENTURA 4). 

One other cool sulphur spring in Matilija Canyon has been men- 
tioned in the description of Vickers Hot Springs. It rises at the 
base of the canyon side, about a quarter of a mUe southeast of the 
Vickers Hot Springs and supphes a cool, strongly sulphureted pool of 
small discharge that was formerly used as a drinking basin. When 
visited, however, it had apparently been unused for several years. 

The region is composed of shales and sandstones that are probably 
of Tertiary age. They are steeply inclined, showing that intense 
folding has taken place. The sulphur constituents of the mineral 
springs in the canyon, as in many other places, are probably derived 
from sulphide and sulphate minerals in the sediments. 

SULPHUR SPRING NORTHEAST OF NORDHOFF (VENTURA 8). 

A small sulphur spring on the hillside about 2f miles by road 
northeast of Nordhofl^ is probably the one that has been sometimes 
referred to as Ojai Sulphur Spring. It is situated in private grounds 
on a gentle open slope about 100 yards north of a ravine and rises in a 
board-curbed pool 5 feet square and 3 feet deep. Bubbles of gas 
intermittently rise in it. The water has a distinctly sulphureted 
odor and taste and the dark color of "black sulphur" waters. Small 
amounts of sulphur are deposited on leaves and other objects that 
expose the sulphide constituents to oxidation by the air. The water 
has been used mainly for laundry purposes at the spring. There is 
said to be a similar spring a mile eastward, and small sulphur springs 
probably issue at other places in this region of Tertiary sediments. 
The rocks of the locahty consist of marine sediments, mainly sand- 



SULPHUR SPRINGS. 



279 



stones, that are of the same character as those in Matilija Canyon 
5 or 6 miles westward. 

SULPHUR MOUNTAIN SPRINGS (VENTURA 9). 

Sulphur Mountain Springs are in the canyon of Sisar Creek, a 
quarter of a mile above (west of) its junction with Santa Paula 
Creek and 6 miles north of Santa Paula. The property has been 
conducted as a summer resort since the late nineties, accommoda- 
tions being provided mainly by tents and tent cottages. The build- 
ings are situated in a grove of black walnuts in a flat on the south side 
of the creek. 

The main spring is on the hillside a few hundred yards southward 
from the grounds and 150 feet above them. It issues from a drift and 
tunnel in a small ravine and 3delds about 15 gallons a minute of 
mildly sulphureted water. The water is conducted in an open 
trough to a storage tank about 50 yards away and is thence piped to 
the grounds to supply a swimming plunge and also tub baths, for 
which it is heated. It issues clear but becomes milky from suspended 
sulphur before reaching the storage tank. The following analysis 
shows it to be a secondary saline water with notable sulphide content: 

Analysis of water from main spring, Sulphur Mountain Springs, Ventura County, Cal. 
[Analyst, Frederick Salathe. Authority, advertisiag matter. Constituents are in parts per million.] 



Temperature 

Properties of reaction: 

Primary salinity 

Secondary salinity 

Tertiary salinity 

Primary alkalinity 

Secondary alkalinity 

Tertiary alkalinity 

Constituents 

Sodium (Na) 

Litliium (Li) 

Calcium (Ca) 

Magnesium (Mg) 

Iron (Fe) •. 

Aluminum ( Al) 

Sulphate (SO^) 

Chloride (CI) 

Sulphide (S) 

Carbonate (CO3) 

Silica (SiOa) 

Hydrogen sulphide (H2S) 




A second spring, which yields perhaps 1 gallon a minute, issues 
near the side of the creek on the resort grounds. An excavation 
6 feet below the ground surface has been cemented, and the water 
rises in a joint of tile pipe that forms a drinking basin. This water 
is not so strongly sidphureted as is that of the larger spring. At 



280 



SPEIITGS OP CALIPOENIA. 



the springs there is a small anticline or upward fold ^ in the Tertiary 
sediments that predominate in this part of the State. At the larger 
spring shaly sandstone is exposed in the tunnel, the walls of which 
are impregnated with alum salts. Small amounts of Hme carbonate 
appear in the cut in front of the tunnel and more noticeable deposits 
of the same material on the hillside below it. 

SFLPHTJR SPRING IN SANTA SUSANA MOUNTAINS (LOS ANGELES 3). 

A spring that is strongly charged with hydrogen sulphide issues 
on the southern side of Santa Susana Mountains, on the Sparks 
ranch, about 5 miles north of Chatsworth. In the early days it was 
visited by the padres of Mission San Fernando, a few miles away, 
and by the Indians of the locahty. The following partial analysis 
of its water made a number of years ago shows it to be secondary 
alkaline and primary saline in character: 

Partial analysis of water from sulphur spring in Santa Susana Mountains, Los Angeles 

County, Cat. 

[Analyst, Oscar Loew (1876). Authority, Wheeler report. Constituents are in parts per million.] 



Properties of reaction : 

Primary salinity 

Secondary salinity 

Tertiary saUnity 

Primary alkalinity 

Secondary alkaUnity 

Tertiary alkalinity 

Constituents, 

Sodium (Na) 

Potassium (K) 

Lithium (Li) 

Calcium (Ca) 

Magnesium (Mg) 

Iron(Fe) 

Aluminum (Al) 

Manganese (Mn) 

Sulphate (SO4) 

Chloride (Cl) 

Carbonate (CO3) 

Phosphate (PO4) 

Silica (SiOz) 

Carbon dioxide (CO2) 

Hydrogen sulphide (H2S) 



(?) 



By 

weight. 



104 
Trace. 
Trace. 

203 

Trace. 
Trace. 
Trace. 

161 
Trace. 

338 
Trace. 
Trace. 



806 



Excess. 
50 



Reacting 
values. 



4.53 
Trace. 
Trace. 

10.10 

Trace. 
Trace. 
Trace. 
3.36 
Trace. 
11.27 
Trace. 
Trace. 



2.93 



The spring is still locally known, but its water has not been used 
as much during recent years for medicinal purposes as it was formerly. 
It has strongly impregnated the adj acent soil with sulphur. Another 
seepage of strongly sulphureted water also issues near by. 

1 Eldridge, G. H., and Arnold, Ralph, The Santa Clara Valley, Puente HiUs, and Los Angeles oil dis- 
tricts, southern CaUfornia: U. S. Geol. Survey Bull. 309, PI. 1, 1907. 



SULPHUR SPRINGS. 281 

SULPHUR SPRING NORTH OF CHATSWORTH (LOS ANGELES 4). 

A sulphur ai)rmg whose water is noticeably above a normal tempera- 
ture issues about H miles north of Chatsworth and 200 or 300 yards 
east of the southern mouth of the Southern Pacific railroad tunnel. 
Its water has not been used except for drinking, but its flow is per- 
haps 8 gallons a minute. It issues from the thick-bedded sandstone 
of this portion of the mountains. 

SULPHUR SPRING AT MOUTH OF BELL CANYON (LOS ANGELES 5). 

At Bell's ranch, at the mouth of BeU Canyon, which enters San 
Fernando Valley from the west, there is a sulphur spring of con- 
siderable flow. The spring is inclosed by a stone-walled reservoir 
about 8 by 12 feet across and 6 feet deep and yields strongly sul- 
phureted water that is rendered milky by sulphur in suspension. 
The water is piped to a summer bathhouse near by. It is very soft 
and good for bathing and laundry use. A similar spring that has not 
been improved issues some distance westward up the canyon. Both 
springs apparently emerge from a calcareous bed near the contact 
between beds of lower Miocene sandstone and middle Miocene shale. 

SULPHUR SPRING SOUTH OF BELL CANYON (LOS ANGELES 6). 

A small spring whose water is noticeably sulphureted is situated 
about 2J miles south of the one at the mouth of Bell Canyon. It 
yields a soft water but has been used only for watering cattle. 

SULPHUR SPRING NEAR CARBERRY STORE (LOS ANGELES 7). 

In a ravine near the Carberry store, which is beside the county road 
along the southern border of San Fernando Valley, there is a smaU 
spring whose water is strongly sulphureted and noticeably above a 
normal temperture. The spring has not been developed and has 
been used only as a watering place by cattle. 

SULPHUR SPRING ON TUCKER RANCH (LOS ANGELES 9). 

A spring on the Tucker ranch, beside the wagon road between Cala- 
basas and Santa Monica, yields water that is rather strongly sulphur- 
eted but is soft and otherwise of good quahty, and as water is 
scarce in this part of the Santa Monica Mountains the spring has 
been used for a number of years as a domestic supply. This spring 
and the sulphur springs south of Bell Canyon and near the Carberry 
Store (Los Angeles 6 and 7) issue from middle Miocene shale that 
dips northeastward toward San Fernando Valley. The sulphur con- 
tents of the spring waters are evidently derived from this shale, as 
it contains noticeable amounts of sulphur compounds. 



282 



SPRINGS OP CALIPORNIA. 



SANTA FE SPRINGS (LOS ANGELES 14). 

Three wells that were put down m the coastal plain 15 miles south- 
east of Los Angeles by Dr. J. E. Fulton, during the seventies, obtained 
sulphur water, and as the locality was favorable a hotel was built, a 
swimming plunge was constructed, and the property was early made 
a resort, under the name of Santa Fe Springs, or Fulton Wells. The 
hotel burned a number of years ago, and the plunge has been filled 
up, but when visited in 1908 the place was still conducted in a small 
way as a resort, there being three small cottages and a bathhouse on 
the property. Windmills over two of the wells 100 yards or more 
from the cottages pumped the water into a tank, whence it was piped 
to a heating boiler and to the baths. The third and innermost wellj 
which is near the cottages, was equipped with a hand pump. Water 
from this well was formerly bottled for table and medicinal use. 
The following analysis shows it to be a secondary alkaline and pri- 
mary and secondary saline water that contains a large proportion 
of iron : 



Analyses of water from east well, Santa Fe Springs, Los Angeles County, Cal. 
[Constituents are in parts per million.] 



Properties of reaction: 

Primary salinity 

Secondary salinity. . . 

Tertiary salinity 

Primary alkalinity. . . 
Secondary alkalinity . 
Tertiary alkalinity. . . 



20 

30 



. 

50 

High. 



24 

31 





45 

High. 



Constituents. 



weight. 



Reacting 
values. 



By 
weight. 



Reacting 
values. 



Sodium (Na) 

Calcium (Ca) 

Magnesium (Mg). 

Iron (Fe) 

Sulphate (SO4)... 

Chloride (Cl) 

Sulphide (S) 

Carbonate (CO3). 
SUica(Si02) 



205 
50 
97 
294 
100 



3.63 
10.21 
4.08 
3.47 
6.12 
2.81 



374 
42 



12.46 
1.39 



90 
167 
47 
107 
a 278 
108 

6.3 
320 



3.89 
8.31 
3.86 
3.84 
5.78 
3.05 
.39 
10.68 



1,246 



1,123.3 



Carbon dioxide (CO2) 

Hydrogen sulphide (H2S) . 



Excess. 
Excess. 



Excess. 
Excess. 



o Reported as "sulphur;" recalculated from CaSO^ by comparison with the other analysis. 

1. Analyst and authority, Winslow Anderson (1888). 

2. Analyst, Price and Hewston. Authority, U. S. Geol. Survey Bull. 32. 

A number of other wells in this coastal plain area of southern Cal- 
ifornia yield water that is noticeably sulphureted but not so strongly 
mineraUzed as is the water of Santa Fe Springs. Seepages of sulphu- 
reted water also issue from shales at a few places along the coast. 
One strongly sulphureted spring of this character issues from the 



SULPHUR SPRINGS. 283 

Cretaceous shales of Point Loma, but as it is exposed only at low 
tide its existence is known to very few people. 

SULPHUR SPRING SOUTHEAST OF CARBON (SHASTA 10). 

There are a few isolated cold sulphur springs in the Cascade- 
Sierran ranges of the State. iVmong them is a small cool sulphur 
spring that issues about 1 mile southeast of Carbon post office in 
Shasta County, a short distance east of Hat Creek. The water flows 
only a few yards from its source and is seldom used for drinking, but 
the spring is of interest because noticeably sulphureted waters are 
uncommon in this part of the State, where the surface rocks consist 
almost entirely of lavas. 

SULPHUR SPRING NEAR HEAD OF BATTLE CREEK MEADOWS (TEHAMA 3). 

Near the head of Battle Creek Meadows and about IJ miles north- 
east of Mineral post office, which is near the southern base of Lassen 
Peak, is a small cool sulphur spring. It issues in a ravine, 15 yards 
from the eastern bank of the creek and 150 yards east of the stage 
road. In 1910 there was a House between the creek and the road, 
and the spring had been cleaned out and was used for drinking. It 
yields about 8 gallons a minute of cold, noticeably sulphureted water 
which deposits small amounts of sulphur. 

The rock that is exposed along the creek is the basaltic lava of 
Lassen Peak. It is worthy of mention that this is the only cold 
sulphur spring that was seen in the Lassen Peak region, the other 
sulphur springs being of notably thermal character. 

McLEAR SULPHUR SPRINGS (PLUMAS 15). 

On the southeast side of Mohawk Valley, near the southern border 
of Plumas County, is a group of sulphur springs that might as prop- 
erly be described with the hot springs, for five of the eight springs 
that rise here are warm, but they are best known as sulphur springs, 
though they are also indicated as thermal on Plate III (in pocket). 

The principal springs are situated a short distance back of the 
buildings on the McLear ranch, rising for a space of about 500 yards 
along the eastern border of the vaUey from lake sediments that have 
been described by Turner.^ The southernmost of these springs 
issues from two vents about 4 yards apart in a bank of sandstone, 
and yields about 8 gallons a minute of water 84° in temperature. 
A second warm spring that rises 100 yards northward in a cut in the 
bank yields about the same amount of water whose observed temper- 
ature was 85°. About 85 yards farther to the northeast a spring 
that yields approximately 30 gallons a minute, of water with a tem- 

1 Turner, H. W., Philos. Soc. Washington Bull., vol. 11, pp. 385-410, 1891. 



284 SPEINGS OP CALIPORN'IA. 

perature of 86°, issues from another adit or cut in the lake sandstone. 
In a small drainage ravine 150 or 200 yards farther northward a 
small sulphureted spring emerges at the base of tuffaceous agglom- 
erate that borders the valley at this point. Near it a cooler spring 
that is not noticeably mineralized rises in a ditch that discharges 
perhaps 5 gallons a minute. The largest spring is 50 yards farther 
up the ravine, where approximately 75 gallons a minute of non- 
mineral water 62° in temperature rises in a small box-curbed pool 
and is piped to the house. The northernmost spring rises from a 
small fissure in the lake sediments and yields perhaps 15 gallons a 
minute of water 85° in temperature. It is mildly sulphureted and 
is distinctly minerahzed, probably mainly with sodium salts. In 
1890 Turner ^ noted a uniform temperature of 75° in the springs but 
mentions the reported increase of temperature of other thermal 
springs in the region at the time of a slight earthquake. He con- 
siders the consolidation of the lake sediments to a sandstone near 
the springs to be due to the cementing action of their waters. The 
water from the several warm springs is collected in a ditch that runs 
below them and is used for irrigation. 

In the meadowland half a mile west of the sulphur springs there 
is a marshy area 20 yards in diameter. A keg that has been sunk 
near its margin affords a drinking pool containing distinctly sul- 
phureted water that had an observed temperature of 48° (in Sep- 
tember). The sulphur contents of this spring and of the warm 
springs seem to be derived from the lake sediments through which 
they rise. 

SULPHUR SPRINGS NEAR SOUTH FORK OF YUBA RIVER (PLACER 2). 

In the canyon of South Fork of Yuba River, less than a mile north 
of Cisco railroad station, are two small springs, one of which forms 
a drinking spring near the wagon road on the southern side of the 
river. The other is some distance farther upstream, on the northern 
side of the river, and has been little used. Their waters are only 
faintly sulphureted. The rocks of the locality consist of slates, in 
part altered by contact metamorphism,^ that are of Jurassic and 
Triassic age. 

SULPHUR SPRING ON BEAR RIVER (NEVADA 1). 

A sulphur spring that is similar to the springs near Cisco rises 
on the northwest bank of Bear River, a quarter of a mile below the 
wagon bridge 3 miles north of Colfax. The spring rises below flood- 
water mark, at the base of a bowlder of gabbro, which is the country 

1 Op. cit., p. 396. 

2 Lindgren, Waldemar, U. S. Geol. Survey Geol. Atlas, Colfax folio (No. 66), 1900. 



SULPHUR SPRINGS. 285 

rock at tliis locality/ and forms a pool of distinctly sulphureted 
water. The spring is known locally, but as it is not near the road 
it has been seldom visited. 

SULPHUR SPRING ON MIDDLE FORK OF AMERICAN RIVER (PLACER 10). 

A small spring of strongly sulphureted water is situated in the 
canyon of Middle Fork of American River, about 20 miles west of 
Tahoe. The water issues at the base of a bluff of morainal material, 
on the southeast side of the stream. It has been visited by fisher- 
men and others who penetrate this portion of the Sierra, but it is not 
well known. 

SULPHUR SPRINGS ON RUBICON RIVER (ELDORADO 1). 

On the southern side of the canyon of Rubicon River, below the 
mouth of Five Lakes Creek and about 13 miles in a direct hne south- 
west of Tahoe, there is a spring that yields perhaps 1 gallon a minute 
of strongly sulphureted, saHne water. Two other similar springs 
issue at points about 1 mile and 3 miles farther downstream. An 
analysis of water from one of them shows that it contains large 
amounts of sodium, calcium, and chloride. As the canyon is rugged 
and is not easily accessible, the springs are not well known. 

The canyon sides near the springs are of granitic rock, but slate 
and quartzite are exposed on the higher slopes, and it seems probable 
that the chemical constituents of the water are derived mainly from 
these altered sedimentary rocks. 

SULPHUR SPRING NEAR AMERICAN RIVER (ELDORADO 5). 

Near Kyburz station, which is on the stage road between Placer- 
ville and Lake Tahoe and near the junction of the Silver and South 
forks of American River, there is a small, strongly sulphureted spring, 
which is known only locally. It is situated in an area of slates and 
granitic rocks that are overlain by lava of relatively recent age, and 
the water probably rises in altered slates near the zone of contact 
with the granitic material. 

SULPHUR SPRING ON PAOHA ISLAND (MONO 6). 

On the western shore of Hot Spring Cove on Paoha Island, in Mono 
Lake, opposite the hot springs that have been previously described 
(IVIono 7, p. 144), there is a spring of mildly sulphureted water that 
has also a slight odor and taste of petroleum. On accoimt of the 
intensely alkalme character of the lake water, this sprmg has at times 
furnished a welcome supply, and during the fall of 1908 it was used 
by men who were drilling for oil on the western border of the island. 
It is worthy of note that a slight artesian flow of warm water, which, 
like the spring water, tasted mildly of hydrogen sulphide and of 

1 Lindgren, Waldemar, op. cit. 



286 SPRINGS OP CALIFORNIA. 

petroleum, was struck at a considerable depth in the well. Both 
the water of the well and that of the spring issue from lake sediments 
which cover the western part of the island. 

SULPHUR SPRING IN SULPHUR MEADOWS (FRESNO 6). 

A spring of faintly sulphureted water rises in Sulphur Meadows, 
one-half mile south of Shaver lumber mills, in the mountains of north- 
eastern Fresno County, It is situated at the border of a pine grove 
in which there is a group of cabins, and it has been curbed and inclosed 
to form a drinking pool. It yields a small amount of clear cool 
potable water. The region is one of granitic rocks, in which at least 
one other sulphur spring rises in the ravine above the meadow, but 
this latter spring is of slight flow and has not been improved. 

SULPHUR SPRINGS NEAR GLENNVILLE (KERN 6). 

Two mildly sulphureted springs that yield a combined flow of about 
10 gallons a minute issue one-half mile east of Glennville post 
office on the slopes of the southern Sierra. The springs have been 
used for irrigating a garden, as their water is not strongly mineralized. 
A few other mildly sulphureted springs of small flow issue in the 
same locality, one of them being near the post office. The rocks of 
the region consist of the granitic material that composes most of 
this portion of the Sierra, and on account of the scarcity of other 
mineralized springs in the vicinity the sulphur springs near Glennville 
are worthy of special note. 

SULPHUR SPRINGS NEAR BULLION MOUNTAINS (SAN BERNARDINO 43). 

Several springs of strongly sulphureted water issue near the southern 
end of BuUion Mountains, in flat land on the road that leads south- 
eastward from Victorville to Dale mining camp. The yield of water 
is considerable, but it tastes too strongly of hydrogen sulphide to be 
palatable. It is seldom used for watering, as there is better water 
about 2 miles farther north. 

SUMMARY OF SULPHUR SPRINGS. 

In the following Hst the sulphur springs, numbering 72, have been 
tabulated, as were the hot springs and the carbonated springs, with 
respect to the character of the rock in which they rise. Many of the 
hot springs are sulphureted, and those which are notably so have been 
included in the list in itaUcs. A few sulphur springs at groups that 
have been described xuider other headings are also included in the list, 
in which they are marked by parentheses. 

The list shows that most of the sulphur springs are in areas of 
sedimentary rocks, possibly because the sulphide constituent, which 
is usuafly hydrogen sulphide, is more readily taken into solution 
from sediments, for they usually contain organic matter and metallic 



SULPHUR SPRINGS. 287 

sulphides from which the hydrogen sulphide is derived, and the 
metaUic sulphides are probably more readily decomposed in the 
relatively pervious shales and sandstones than they are in the rela- 
tively impervious crystalline rocks. 

Sulphur-spring localities.^ 

In alluvium. 
Byron Hot Springs. 
Sulphur springs on Burton Mound. 
Santa Fe Springs (wells). 
Sulphur spring on Pacha Island. 
Sulphur springs near Bullion Mountains. 

In sandstone or shale. 

St. Helena White Sulphur Springs. 

O'Donnells Springs. 

Wall Springs. 

Sulphur springs in Franz Valley. 

Sulphur spring near Little Sulphur Creek. 

Sulphur spring near Sulphur Creek. 

The Geysers. 

Little Geysers. 

Sulphur springs on branch of Deep Creek. 

Muir Springs. 

Sulphur spring near branch of Eel River. 

Sulphur springs near Cumminga. 

Sulphur spring near Hoaglin. 

Sulphur spring in Eureka. 

Mountain View Spring. 

Cook Spring. 

Sulphur spring southwest of Fouts Springs. 

Sulphur spring west of Fouts Springs. 

Wilbur Hot Springs. 

Jones Hot Springs. 

Sulphur spring near Blue Lakes. 

Hayvilla Sulphur Spring. 

(Saratoga Springs, one sulphur spring.) 

(Tuscan Springs, sulphureted saline springs.) 

(Richardson Springs, sulphureted saline springs, from tuffs.) 

Sulphur springs in Sulphur Valley. 

Harbin Springs. 

Anderson Springs. 

Zem Zem Spring. 

Sulphur springs near Walnut Creek. 

Sulphur spring in Pine Canyon. 

Mayhew Spring. 

(Alum Rock Park Springs, several sulphur springs.) 

Paraiso Hot Springs. 

Sulphur spring on Crow Creek. 

Sulphur springs on Orestimba Creek. 

Hinns Sulphur Spring. 

1 Thermal springs are in italics; those described in other groups are in parentheses. 



288 SPRINGS OF CALIFORNIA. 

Olive Spring. 

Sulphur spring on Bodfish Creek. 

Blodgett Magic Spring. 

El Pajaro Springs. 

Sulphur spring on Mission Greek. 

Sulphur spring in Carrizo Plain. 

Pecho Warm Springs. 

San Luis Hot Springs. 

San Marcos Hot Springs. 

Montecito Hot Springs. 

Vickers Hot Springs. 

Stingleys Hot Springs. 

Lyons Spring. 

Sulphur spring in Matilija Canyon. 

Matilija Hot Springs. 

Wheelers Hot Springs. 

Sulphur spring northeast of Nordhoff. 

Sulphur Mountain Springs. 

Sulphur spring in Santa Susana Mountains. 

Sulphur spring north of Chatsworth. 

Sulphur spring at mouth of Bell Canyon. 

Sulphur spring south of Bell Canyon. 

Sulphur spring near Carberry store. 

Sulphur spring on Tucker ranch. 

McLear Sulphur Springs. 

In metamorphic rocks. 

Vallejo White Sulphur Spring. 

Sulphur spring near Laytonville. 

Deerlick Springs. 

Sulphur springs on Browns Creek . 

Neys Springs. 

Sulphur spring on Castle Creek 

Colyear Springs. 

Hensley Spring. 

Sulphur spring on South Fork of Cottonwood Creek. 

Piedmont Springs. 

Blodgett Mineral Spring. 

Sulphur springs near South Fork of Yuba River. 

In lava. 
Napa Vichy Spring. 
El Toro Spring. 
Taylor Sulphiir Spring. 
Hillydale Sulphur Spring. 
Sulphur spring southeast of Carbon. 
Sulphur spring near head of Battle Creek Meadows. 
Hot springs on Bidwell Creek. 

In granitic rocks. 
Huer Huero Springs. 
Sulphur spring on Bear River. 
Sulphur spring on Middle Fork of American River. 
Sulphur springs on Rubicon River. 
Sulphur spring near American River. 



SALINE SPRINGS. 289 

Sulphur spring in Sulphur Meadows. 
Sulphur springs near Glcnnville. 
Wai-m spring in Panamint Valley. 
Tassajara Hot Springs. 
San Jacinto Hot Springs 

SALINE SPRINGS. 

NUMBER AND DISTRIBUTION. 

California contains no large saline springs nor wells that yield 
brine which furnishes a commercial supply of common salt, but a 
number of small, notably salme springs issue in the northern part 
of the Coast Ranges, most of them in areas of unaltered sediments of 
Tej'tiary and Cretaceous age. In the earlier slates of the northern 
Sierra there are a few salt licks, or deer licks, and a few strongly 
saline and alkaline springs also rise in the deserts of the southeast- 
ern pai't of the State, where great evaporation has concentrated 
the salts that have probably been leached from ancient sedimentary 
rocks. Several of the springs have been commercially developed, 
either as resorts or for the purpose of bottling the water. In the 
following pages the developed springs are first described, beginning 
with those in the northern part of the State. 

TUSCAN SPRINGS (TEHAMA 5). 

Tuscan Springs (PL XII, B, p. 200) are 10 miles northeastof Red 
Bluff near the head of the canyon of Salt Creek. They are said to 
have received their name because. when they were fix'st noticed a 
salt that coated the surface resembled that at Tuscan, Italy. It is 
also said that the first borax in the State was found here and that 
borax has been found in the spring waters,^ but borates are not 
reported in the available analyses. The property was early improved 
as a resort for the medicinal use of the water, and a three-story 
hotel and a bathhouse were erected. In 1909 a large cottage and 
several smaller ones furnished additional accommodations; gas from 
one of the springs was used for lighting, and water from another 
was evaporated in shallow troughs and the salt was sold for medicinal 
use. The water was formerly bottled and marketed, but the sale 
of the salt has replaced the trade in the water. 

The canyon of Salt Creek widens at its head to a small valley or 
amphitheater, surrounded by rugged cliff's, ^ and the springs issue 
along the main creek and its branches m this open area. As many 
as 52 springs have been claimed for the locality, but the writer 

' California State Mineralogist Tenth Kept., p. 694, 1890. 

2 On account of its shape and its walls of tuffaceous lava, the locality has been described (California State 
Mineralogist Tenth Rept., pp. 693-694, 1890) as a volcanic crater, but the shales in the bottom of the am- 
phitheater discountenance this hypothesis. 

35657°— wsp 338—15 19 



290 



SPRINGS OF CALIFORNIA. 



counted only 18 appreciable springs. Spring houses protect the 
three that are most used for drinking. Water from another spring 
supplies the evaporating trays. Two other springs rise in cemented 
reservoirs about 15 and 20 feet in diameter. Gas from one of these, 
which is called the Natural Gas Spring, is piped to a tank higher 
on the hillside for use at the hotel, and water from the other, which 
is named Fountain Spring, supplies the baths. The other springs 
rise in bricked and cemented basins along the banks of the drainage 
channels. All of the springs are within 250 yards south to east of 
the hotel, which is on higher ground overlooking them. Most of 
them are of inappreciable flow, but all are strongly mineralized. 
Some are strongly sulphureted as well as saline^ and for this reason 
the locality is marked on Plate III (in pocket) as one of sulphur springs. 
The following analyses indicate that they are primary saline waters 
remarkably uniform in composition for springs of such high mineral 
content, the chief difference being in the high sulphate content of 
spring No. 1. The remarkably high potassium content in all but 
the Natural Gas Spring is notable. It is not unlikely that the pro- 
portion of potassium is about the same for all the springs and that 
the apparent difference is due to differences in analytical methods 
or calculation. 

Analyses of water from Tuscan Springs, Tehama County, Cal. 
[Authority, advertising matter. Constituents are in parts per million.] 



Properties of reaction: 

Primary salinity 

Secondary salinity. . 

Tertiary salinity 

Primary alkalinity. . 
Secondary alkalinity 
Tertiary alkalinity . 



Constituents. 



43 ^ 



■9.0 






•a CO 

O -3 



1) (> 



•3^ 

o 3 






■■Hs 



Sodium (Na) 

Potassium (K)... 

Lithium (Li) 

Barium (Ba) 

Calcium (Ca) 

Magnesium (Mg). 

Iron (Fe) 

Sulphate (SO4)..- 

Chloride(Cl) 

Carbonate (CO3). 
Silica (Si02) 



8,096 

29 

.3 

3.7 

144 

92 

13 

351 

12, 460 

281 

35 



352.0 

.75 

.05 

.05 

7.20 

7.59 

.47 

7.30 

351.4 

9.38 

1.17 



8,349 

2,448 
L7 



363.0 
62.6 

.24 



8,241 
3,353 
2.0 



358.3 

85.8 
.29 



7,944 
2,705 
1.9 



345.4 

69.2 

.27 



8,386 
2,851 
L9 



364.6 
72.9 

.27 



67 
23 

2,108' 

13, 540 

156 

13 



3.34 

1.86 

.03 

43.9 

381.9 

5.20 

.43 



66 

28 

Trace. 

420 

15,440 

166 

13 



3.28 
2.27 
Tr 
8.76 
435.6 
5.55 
.43 



27 

Trace. 

448 

14,380 

167 

5.6 



3.37 
2.21 
Tr. 
9.33 
405.6 
5.58 
.19 



21 



680 

15,020 

154 



3.41 

1.71 

.00 

14.15 

423.6 

5.12 

.02 



21,505.0 



26,706.6 



27,729.0 



25, 746. 5 



Hydrogen sulphide (H2S) . 



383 



22.54 



320 



18.77 



122 



7.16 



17.23 



1. Natural Gas Spring. Analyst, Price & Son. 

2. Spring No. 1. Analyst, N. Lehnen (1905). 

3. Spring No. 10. Analyst, N. Lehnen (1905). 

4. Spring No. 11. Analyst, N. Lehnen (1905). 
-5. Spring No. 15. Analyst, N. Lehnen (1905). 



SALINE SPRINGS. 



291 



The following analysis of the marketed salt indicates that the water 
from wliich it is derived has a somewhat different composition from 
that of the other springs, and the absence of calcium and magnesium 
from it seems questionable. The average proportion of the soluble 
materials in ocean water is tabulated with it, for comparison. 

Analyses of Tuscan Springs salts and soluble matter in ocean water. 



Tuscan 
Springs 
salts.o 



Ocean 
water. b 



Sodium (Na'> 

Potassium (K)... 

Lithium (Li) 

Calcium (Ca) 

Magnesium (Mg). 
Sulphate (SO4)... 

Chloride (01) 

Bromide (Br) 

Carbonate (CO3) . 



28.05 

15.50 

.02 



30.65 
Lll 



.62 
55.77 



1.20 

3.75 

7.68 

55.20 

.20 

.21 



100.10 



100.00 



Analyst, N. Lehnen (1905). Authority, advertising matter. 

6 Recalculated from average composition of ocean water: Dittmar, Challenger Reports, Physics and 
chemistry, vol. 1, p. 204, 1884. 

The springs rise in dark-colored shale and sandstone, the latter 
material being veined in places with calcite. The structure shows 
that the beds have been folded into a small arch or anticUne at this 
locality. Dips of 50° on the western side of the fold were observed. 
The occurrence of usable quantities of illuminating gas is worthy of 
mention in connection with this anticHnal structure, as is also the 
presence of a large mound, shown in Plate XII, B (p. 200). This 
mound has the appearance of a spring formation, although the 
material on its surface was not noticeably different from that of the 
adjacent slopes. The sediments are overlain by volcanic agglom- 
merate or tuff, which forms the cUffs of the canyon walls. The 
marine sediments have been described by DiUer ^ as part of the 
Chico formation, of Upper Cretaceous age, and the fresh-water 
deposit of tuffaceous material that overhes them has been named the 
Tuscan tuff and is of Pliocene age.^ 

RICHARDSON SPRINGS (BUTTE 2). 

Richardson Springs are situated in the canyon of Mud Creek, 12 
miles north of Chico. The property has been developed as a medicinal 
and vacation resort since 1898. In 1909 the improvements included 
a main hotel, three large rooming cottages, a number of small ones, 
and a bathhouse. The buildings are on the slope on the northern side 

1 Diller, J. S., Geology of the Lassen Peak district: U. S. Geol. Survey Eighth Ann. Rept., pt. 1, p. 411, 
1889; Tertiary revolution in the topography of the Paciflc coast: U. S. Geol. Survey Fourteenth Ann. 
Rept., pt. 2, pp. 40.5-400, 1894. 

2 Diller, J. S., Geology of the Lassen Peak district: U. S. Geol. Survey Eighth Ann. Rept., pt. 1, pp. 
422-424, 1889. 



292 



SPEINGS OF CALIFORNIA. 



of the creek, and the springs issue along the northern edge of its 
natural channel. A wall directs the stream to the opposite side of its 
channel, however, and protects the springs from being flooded. 

Three of the four principal springs on the property rise within 30 
yards of each other, between the hotel and the bathhouse. Two of 
these form cemented drinking pools of slight discharge in which the 
water is strongly saline and sulphureted. The analysis of the water 
of the western of these two (No. 1 below) indicates that it is a highly 
concentrated sahne water. The central spring of the three rises in a 
concrete standpipe to a height of several feet above the ground, and 
its water is thence conducted by a small flume to a heating boiler at 
the bathhouse. Small quantities of sulphur and gypsum are deposited 
along the sides of the flume. The yield is about 2^ gallons a minute. 
The fourth spring, which is known as Montgomery Spring, rises in a 
cemented drinldng pool about 300 yards farther eastward, upstream, 
and yields perhaps 2 gallons a minute of mildly sulphureted water 
that does not taste noticeably saline. Analysis shows that it is a 
moderately concentrated water of primary and secondary alkaline 
character but containing also notable primary salinity. Because of 
the sulphureted character they are indicated on Plate III (in pocket). 

Analyses of water from Richardson Springs, Butte County, Cal. 
[Analyst, Maxwell. Authority, advertising matter. Constituents are in parts per million.] 



Temperature 

Properties of reaction: 

Primary salinity 

Secondary salinity . . . 

Tertiary sallnit;^ 

Primary alkalinity. . . 
Secondary alkalinity . 
Tertiary alkalinity . . 



Spring No. 1. 



16° C. (61° P.). 

90 
10 
Trace. 


9 



Montgomery Spring. 



15° C. (59° P.). 

30 


25 
45 
45 



Constituents. 



By 
weight. 



Sodium (Na) 

Potassium (K) 

Lithium (Li) 

Ammonium (NH4). 

Barium (Ba) 

Calcium (Ca) 

Magnesium (Mg). . . 

Iron (Fe) 

Aluminum ( Al) 

Sulphate (SO4) 

Chloride (01) 

Carbonate (CO3).. . 
Silica (SiOz) 



Carbon dioxide (CO2) 

Hydrogen sulphide (H2S) . 



6,431 
766 
Trace. 
Trace. 



622 

11 

Trace. 

6.3 

2,730 

9,729 



18 



20, 313. 3 



96 

417 



Reacting ' By 
values. weight. 



279.2 

19.6 

Trace. 

Trace. 



31.05 

.92 

Trace. 

.71 

56.9 

274.6 



.60 



4.36 

24.48 



89 

18 

Trace. 



Trace. 

48 

14 

Trace. 

3.7 

66 

36 

165 

61 



500.7 



Reactrag 
values. 



3.87 

.46 

Trace. 



Trace. 
2.39 
1.15 

Trace. 
.41 
1.37 
1.01 
5.50 
2.02 



.50 
1.02 



SALINE SPRINGS. 293 

A cemented drinking basin surrounds a fifth spring, known as the 
Iron Spring, on the side of a ravine about 400 yards north of the main 
springs. The overflow is shght and the water has no distinctly min- 
eraHzed taste. 

In several respects conditions at Richardson Springs are similar 
to those at Tuscan Springs, about 35 miles farther north. As at 
Tuscan Springs, clifTs of lava agglomerate form the upper portion of 
the canyon side, but the springs issue from tuffaceous sediments 
(the Tuscan tuff) that overlie the Cretaceous shales and sandstones 
which are exposed at Tuscan Springs and which probably underlie 
the tuft' at a shallow depth at Richardson Springs. About three- 
quarters of a mile southwest, downstream from the springs, inflam- 
mable gas rises near the creek, probably from these Cretaceous beds. 
In December, 1909, an attempt was being made to confine the gas 
and render it available for use. 

SALINE SPRINGS AT BYRON HOT SPRINGS (CONTRA COSTA 8). 

Byron Hot Springs have been described among the thermal springs, 
but they are mentioned here because the waters of two of them — the 
Liver and Kidney and the Hot Salt springs — are notably saline, and 
that of Surprise Spring is a strong brine. Comment on the saUne 
character of these springs was made in describing the group. (See 
p. 109.) 

ALHAMBRA SPRINGS (CONTRA COSTA 2). 

At two localities in the State there are small saline and sulphated 
springs whose waters have been bottled for medicinal use. Although 
not all of the springs at these locaUties are notably sahne, the principal 
springs contain large amounts of sodium and chlorine, and the locali- 
ties may properly be considered with the saline springs. 

The northern locality is at Alhambra Springs, which are situated 
in a ravine about 6 miles by road south of Martinez. Of the three 
principal springs on the property, one which is known as No. 1, fills 
a housed-in pool 6 feet square and a foot deep, on the eastern bank 
of the ravine; its water tastes strongly saUne and sulphated. About 
400 yards southward, up the ravine from it, a mildly sulphureted 
spring rises in a small spring house. The third spring, which is known 
as Spring No. 2, rises in a cement-covered joint of tile pipe on the 
western edge of the stream channel, 75 yards above this sulphur 
spring. Water from the two numbered springs is piped to tanks 
and thence to bottUng works beside the raiboad at Martinez, A 
fourth spring has a flow of a little over half a gallon a minute and is 
designated in the table of analyses as "Alhambra." The following 
analyses show that the waters of the Alhambra and Spring No. 1 
are primary and secondary saline in character, but the water of Spring 



294 



SPEINGS OF CALIFOElsriA. 



No. 2 is less strongly mineralized than that of the others and is char- 
acterized chiefly by secondary alkahnity. 

Analyses of ivater from Alhambra Springs, Contra Costa County, Cal. 
[Authority, advertising matter. Constituents are in parts per million.] 



Temperature 

Properties of reaction: 

Primary salinity 

Secondary saUnity . . . 

Tertiary salinity 

Primary alkalinity. . . 
Secondary alkalinity . 
Tertiary alkalinity . . . 



14° C. (57° F.) 

73 
26 


1 
3 



9° C. (48° F.) 

63 

36 





1 

Trace. 



Constituents. 



By 
weight. 



Reacting 
values. 



By 

weight. 



Reacting 
values. 



By 
weight. 



Reacting 
values. 



Sodium (Na) 

Potassium (K) 

Lithium (Li) 

Ammonium (NH4) 

Bariuni (Ba) and strontiimi (Sr) . 

Calcium (Ca) 

Magnesium (Mg) 

Iron(Fe) 

Aluminum ( Al) 

Manganese (Mn) 

Sulphate (Sd) 

Nitrate (NO3) and nitrite (NOo) . 

Chloride (CI) 

Bromide (Br) 

Iodide (I) 

Sulphide(S) 

Carbonate (CO3) 

Metaborate (BO2) 

Arsenate ( ASO4) 

Phosphate (PO4) 

SiUca(Si02) 



Carbon dioxide (COo) 

Hydrogen sulphide (H2S) . 



3,416 



148. 52 
L74 



100 
13 



4.34 
.32 



972 
106 
9.5 

5.8 



48.49 

8.72 

.34 

.64 



4.07 
3.43 



2,727 
7.6 
.8 
L3 

1,278 
81 



60 
"7,' 265' 



1.24 

'263.' ig 



2.2 

'iso"" 

"32"" 



.24 
'3.'75 
".'91' 



1.] 

35 

Trace. 

6,595 

21 

13 



118. 57 
.19 
.01 

.07 
.00 

63.78 
6.77 

.02 

.04 
.73 

Trace. 

185. 98 
.26 
.10 



3.68 
.34 



51 

26 



Trace. 

20 



1.70 
.61 
.00 
Trace. 
.66 



689.2 



10, 858. 4 



Present. 



Present. 



5.5 




.25 
.00 



• 1. Spring No. 1. Analyst, Thomas Price & Son. 

2. Spring No. 2. Analyst, Thomas Price & Son. 

3. ALhambra Spring. Analyst, Curtis and Tompkins. 

The waters have been on the market since about 1898, and have 
been bottled, both carbonated and still (natural), A ''tonic water," 
consisting of 25 per cent of No. 1 and 75 per cent of No. 2, has also 
been marketed. 

The rocks near Alhambra Springs are of the same character as 
those at Ferndale Springs (Contra Costa 1, p. 208) half a mile to the 
northwest, which have been described among the carbonated springs. 
They consist of soft shales and sandstones that are apparently tilted 
about 30° W. 

VERONICA SPRINGS (SANTA BARBARA 3). 

The southern locality of saline or sulphated springs whose waters 
are bottled is in the hills near the coast, 2 or 3 miles west of Santa 
Barbara. The most important of these — Veronica Springs— are 



SALINE SPRINGS. 295 

situated on the sides of the wide drainage channel of San Roque 
Creek, about three-quarters of a mile northward from the ocean. 
The principal springs are on the western side of the creek, but water 
from about 12 springs, half of which are on each slope of the drain- 
age channel, has been piped to collecting tanks in a warehouse at 
the principal springs. As the yield of the springs is small and the 
bottled product consists of the combined flow from a number of springs 
whose com])osition probably varies with the season, differences in 
any two analyses of the water would be expected. The remarkably 
high content of magnesia shown by the analysis on page 296 seems to 
have been produced by concentration of the material from the ocean 
water by some means which is not clearly understood but which prob- 
ably involved the evaporation of the water of lagoons to a bittern, 

BYTHINIA SPRINGS (SANTA BARBARA 4). 

Bythinia Springs issue m a gully on the hillside, half a mile north- 
west of Veronica Springs. The water has been piped to a bottling 
house below them and marketed as a medicinal water, but the com- 
mercial value of the springs has not been so great as that of the 
others to the southeast. 

SANTA BARBARA SPRINGS (SANTA BARBARA 5). 

Santa Barbara Springs are about three-fourths of a mile northeast 
of Veronica Springs, near the top of the mesa land overlooking Santa 
Barbara. Their water, like that of the other strongly mineralized 
springs in the locality, has been marketed to some extent for medi- 
cinal use. Pipes from several small springs supply a bottling plant. 

The following analyses of waters from the three groups of springs 
last described show that they all are primary and secondary saline 
waters, secondary salinity being dominant in Veronica and Bythinia 
springs. 

The flat-topped hills on whose flanks the springs issue are com- 
posed of shales of late Tertiary age that probably belong to the 
Fernando formation, which has been described by Arnold.^ The 
mineralized water is said to seep from a yellow clay of the consist- 
ency of cheese. 

1 Arnold, Ralph, Geology and oil resoxirces of the Sirmmerland district, California: U. S. Geol. Survey 
BuU. 321, pp. 30-33, 1907. 



296 



SPRINGS OP CALIPORNIA. 



Analyses of water from Veronica, Bythinia, and Santa Barbara springs, Santa Barbara 

County, Cal. 

[Constituents are in parts per million.] 



Properties of reaction: 

Primary salinity 

Secondary salinity . . . 

Tertiary salinity 

Primary alkalinity. . . 
Secondary alkalinity . 
Tertiary alkalinity . . . 



- 27 
68 


5 
Trace. 



24 
73 


3 
'i'race. 



63 
23 


14 
Trace. 



Constituents. 



By 
weight. 



Reacting 
values. 



By 

weight. 



Reacting 
values. 



By 

weight. 



Reacting 
values. 



Sodium (Na) 

Potassium (K) 

Lithium (Li) 

Ammonium (NH4). 

Calcium (Ca) 

Magnesium (Mg). . . 

Iron(Fe) 

Aluminum ( Al) 

Manganese (Mn) . . . 

Sulphate (SO4) 

Nitrate (NO3) 

Nitrite (NO2) 

Chloride (CI) 

Bromide (Br) 

Iodide (I) 

Carbonate (CO3) . . . 
Metaborate (B O2) . . 
Arsenate (ASO4)... 
Phosphate (PO4).. - 
Silica (Si02) 



Carbon dioxide (CO2). 



2,153 



93.6 
2.27 



3,210 
21 



139.6 
.53 



4,043 
296 



175.8 
7.58 
.09 



.1 

564 
2,858 

2.6 



12,361 

1,740 



2,004 



Trace. 

522 





Trace. 

18 



Trace. 
28.13 
235.0 



.00 
257.5 
28.1 

.00 

56.5 

.00 

Trace. 

17.41 

.00 

.00 

Trace. 

.60 



561 
4,920 



28.0 
404.7 



856 
773 
8.4 



42.^ 
63.6 
.30 



20, 880 
3,988 



434.8 
64.2 



504 



2 107 

Trace. 

Trace. 
1,206 
1.6 



59.4 
Trace. 
Trace. 

40.2 
.04 



22,311.7 



36, 151 







.65 



18,447.6 



1. Veronica Spring. Analyst, U. S. Bureau of Chemistry (1903-1904). Authority, U. S. Bureau of 
Chemistry Bull. No. 91. 

2. Bythinia No. 3 (bottled). Analysts, Jlilgard, Jaffa and Colby. Authority, advertising matter. 

3. Santa Barbara (bottled). Analyst, Curtis and Tompkins. Authority, advertising matter. 



EPSOM SPUING (LAKE 33). 

A small flow of sulphated water, known as Epsom Spring, formerly 
issued in a ravine about 2^ miles south of west from Lakeport. 
Within recent years range animals have trampled the place so that 
there has been little or no flow, but during the summer a considerable 
efliorescence of Epsom salt forms on the surface of the moist ground, 
and a small flow of water could probably be again developed at the 
place. The locality is near the western border of a belt of serpentine 
that extends northward along the western side of Clear Lake. It 
seems probable that this magnesian rock furnishes the basic portion 
of the efflorescent salt, which may be formed by chemical reaction of 
the minerals dissolved in water that passes through both the serpen- 
tine and the adjacent altered sedimentary materials. 



SALINE SPRINGS. 297 

COMPLEXION SPRINGS (LAKE 14). 

In Lake County and more northern portions of the Coast Ranges 
there are several springs that contain unusually large amounts of 
ammonium salts. It has not been considered advisable to group them 
for discussion according to this characteristic, however, as they have 
other and different qualities. 

Complexion Sprmgs are perhaps remarkable chiefly because of their 
high content of ammonium, but they are also strongly salty and hence 
are described with the salt springs. They include three pools, which 
are situated on the slope 50 yards east of the bed of a ravine about 325 
yards north of the road between Leesville and Hough Springs (Lake 
13, p. 197), and 2 miles west of the divide at the boundary between 
Lake and Colusa counties. The northernmost pool, which is the prin- 
cipal one, is about 4 feet in diameter and 2 or 3 feet deep. A few^ bubbles 
of gas rise at its back edge, beneath a small bank, and the discharge is 
perhaps a quarter of a gallon a minute of clear water that tastes strongly 
of salt and ammonia and that deposits on the sides and bottom of the 
pool a white curdy precipitate that is easily roiled. The analysis shows 
that this precipitate consists chiefly of calcium and magnesium com- 
pounds, and its similarity to the hard deposit at the hot springs at the 
Elgin mine (Colusa 7, p. 104) and at Phillips Soda Spring (Napa 8, 
p. 161) is worthy of note. The water contains an unusually large 
proportion of ammonium and hydroxide, but analysis shows that it is 
really a brine, the other constituents being in very minor amounts 
compared with the sodium and chloride contents : 

Analysis of insoluble deposit in Complexioti Springs, Lake County. 

[Analyst and authority, F. M. Eaton, 1910.] 

Silica (Si02) IS. 67 

Iron and alumina (Fe2()3+ AI2O3) 3. 08 

Lime (CaO) 31. 90 

Magnesia (MgO) 17. 15 

Sulphate (SO4) 

Undetermined (H2O+CO2) 29. 20 

100.00 



298 



SPRINGS OF CALIFORNIA. 



Analysis of ivater from main spring, Complexion Springs, Lake County, Cal. 
[Analyst and authority, F. M. Eaton (1910). Constituents are in parts per million.] 



Properties of reaction: 

Primary salinity 

Secondary salinity 

Tertiary salinity , 

Primary alkalinity 

Secondary alkalinity 

Tertiary alkalinity 

Constituents 

Sodium (Na) 

Potassium (K) 

Ammonium (NH4) 

Calcium (Ca) 

Magnesium (Mg) 

Iron (Fe) 

Aluminum ( Al) 

Sulphate (SO^) 

Chloride (CI) 

Hydroxide (OH) 

Carbonate (CO,) 

Metaborate (BO2) 

Arsenate (AsO^) 

Phosphate (PO4) 

Silica (Si02) 

Carbon dioxide (CO2) 

Hydrogen sulphide (H2S) 



94 


6 

Trace. 

Trace. 



By 
weight. 



Reacting 
values. 



10,295 
223 
150 
6.9 
Trace. 

> Trace. 

47 
15, 400 
178 
456 
Trace. 


2.8 



447. 01 

5.70 

8.31 

.34 

Trace. 

Trace. 



434. 29 

10.47 

15.20 

Trace. 

.00 

.00 

.09 



26, 758. 7 



, The second pool, which is 5 or 6 yards southwest of the main one 
and is somewhat smaller, also yields a shght flow of clear salty 
ammoniacal water, but a precipitate does not form in it. The third 
pool, about 5 yards farther south, was not overflowing when visited 
in July, 1910. It contained brown-stained water that tasted strongly 
of salt but not of ammonia. Water from the principal spring has 
been used locally as a nasal douche and as a wash for sores. 

The water issues from decomposed serpentine, but altered sediments 
are exposed in the ravine near by. Although the yield of Complexion 
Springs is small, their continual flow and strong minerahzation indi- 
cate that their source is deeper and more permanent than would be 
furnished by surface seepage. The chemical character of the water 
indicates that it receives its salt content from the sedimentary beds, 
whereas the ammonia is possibly formed by chemical reactions of the 
minerals of the decomposed serpentine, perhaps by the action of 
ferrous sulphate on organic matter. 

SALT SPRING NORTH OF SITES (COLUSA 4). 

On the Peterson ranch, 3^ miles north of Sites, there is a salt spring 
whose water has been used for many years to supply stock salt for 
the use of the ranch by evaporating the brine in shallow troughs. 
The spring has no surface overflow, as it forms a pool in a salt flat 
where the discharge seeps away, but the quantity of water is sufficient 
to supply several evaporating troughs. The rocks of the locaUty are 



SALINE SPRINGS. 299 

unaltered sediments, mainly sandstone, in which there are apparently 
beds that contain an unusually large amount of salt. 

SALT SPRING IN SALT SPRING VALLEY (GLENN 3). 

A spring that is similar in character to the one north of Sites is 
situated in Salt Spring Valley about 4 miles north of Stonyford or 
27 miles north of west from Sites. The water issues on the slope 
above the valley land and flows down through a barren salty patch 
perhaps 2 acres in extent. No attempt has been made to collect 
the salt in commercial amount, although the spring yields several 
gallons a minute of salty water. The crust that forms naturally is, 
however, occasionally scraped up and used as stock salt. The salt 
of tliis spring, like that of the spring near Sites, is apparently derived 
from salt-bearing layers in the unaltered sedimentary rocks that com- 
pose the hills along the western side of Sacramento Valley. 

SALT SPRINGS WEST OF ELK CREEK (GLENN 2). 

Salt springs issue about 3 miles west of Elk Creek post office, in 
western Glenn County, but they are of small flow and have been 
used mainly as salt licks by range cattle. As seems probable at the 
salt spring farther south, in Salt Spring Valley, those west of Elk Creek 
apparently derive their salt from beds in the unaltered sedimentary 
rocks that form this portion of the Coast Ranges. 

SALT SPRINGS ON NORTH FORK OF ELDER CREEK (TEHAMA 11). 

A few seepage springs of salty water issue on North Fork of Elder 
Creek, about 32 miles by road south of west from Red Bluff. A 
number of years ago a small amount of the water was bottled and 
found a local sale for medicinal use. The springs have not been 
improved nor used in recent years, though they have been considered 
valuable because of their mineral character. The water issues from 
dark-colored shales of the Chico formation of Upper Cretaceous age, 
which has been described by Diller.^ 

SALT SPRINGS ON STEWARTS FORK OF TRINITY RIVER (TRINITY 1). 

A few small springs of salty water that are similar in character to 
those on Elder Creek (Tehama 11) issue along Stewarts Fork of 
Trinity River, in northern Trinity County. They are remote from 
other than mining settlements, however, and have been little used. 
Schists and dark altered shales cover a large part of the area in this 
portion of the Coast Ranges, and it is from such material — probably 
altered sediments — that the saline water issues. 

1 Diller, J. S., Tertiary revolution in the topography of the Pacific coast: U. S. Geol. Survey Fourteenth 
Ann. Rept., pt. 2, pp. 405-406, 1894. 



300 SPRINGS OF CALIFORNIA. 

FELTS SPRINGS (HUMBOLDT 5). 

Felts Springs are situated 5^ miles by road and trail northeast of 
Fortuna. The property was formerly used as a resort, but one hotel 
burned in 1878 and another in 1894, and since that time the place 
has been abandoned. 

The group mcludes three springs that lie close together near the 
top of a hiU from which the timber has been cut. The largest spring 
rises in a reservoir or well 24 feet deep and 6 feet in diameter and 
yields about half a gallon a minute of saline water. One of the other 
springs is also saline, and the third is mildly sulphureted. A small 
amount of gas rises in each spring. 

Soft sandstone that contains fossil shells is exposed near the 
springs and to the south and west there are sand dunes. The saline 
and sulphureted constituents of the waters are evidently derived from 
the marine sediments from which the springs issue. 

SALT SPRINGS ON NORTH FORK OF AMERICAN RIVER (PLACER 9). 

On the western bank of North Fork of American River, .about 2 
miles east of Colfax, there are a few saline and alkaline seepages that 
are known to local hunters as salt licks or deer licks. Springs that 
yield perhaps 10 gallons a minute issue 25 or 30 feet above the river 
from the canyon side. There is said to be a considerable saline deposit 
along their courses in summer, but when the locality was visited the 
small deposit that was seen consisted mainly of soda and alum. The 
surrounding rock is slate of Carboniferous age, which has been described 
by Lindgren.^ The saline material is apparently derived from these 
old sediments. 

VALLEY SPRINGS (CALAVERAS 1). 

Two small saline springs issue about one-half mile east of VaUey 
Springs station on the branch railroad from Lodi eastward into the 
mountains bordering Sacramento Valley. One spring is a mere 
seepage, but the other yields about 1 gallon a minute of water having 
a temperature of 75°. In the summer of 1909 this water was being 
bottled for use as a mineral table water. The following partial 
analysis shows that the water is primary and secondary saline in 
character. 

1 Lindgren, Waldemar, U. S. Geol. Survey Geol. Atlas, Colfax folio (No. 66), pp. 1-2, 1900. 



SALINE SPRINGS. 



301 



Partial analysis of xoater from main spring, Valley Springs, Calaveras County, Cal. 
[Analyst, G. E. Colby (1909). Authority, owner of springs. Constituents are in parts per million.] 



Propertirs of reaction: 

Primary salinily 

Secomlary suliiiily 

Tertiary salinity 

Primary alkalinity 

Secomlary alkalinity 

Tertiary alkalinity 

Constituents. 

Residue soluble in water 

Sodium (Na) 

Potassium ( K) 

Magnesium (Mg) 

Sulphate (SO4) 

Chloride (CI) 

Carbonate (CO3) 

Residue insoluble in water 

Calcium (Ca) 

Magnesium (Mg) 

Sulphate (804) :: 

Carbonate (CO3) 

Silica (Si02) 

Loss on ignition (organic matter and chemically combined water) 

Total residue 



Large. 

Large. 





Moderate. 

Small. 



By weight. 



1,687 

Large. 

Small. 

Considerable. 

Large. 

Large. 

Small. 

843 

Large. 

Large. 

Large. 

Large. 

Large 

324 



2,854 



Several other saline springs that are very probably similar in 
mode of occurrence and chemical character issue at points farther 
south in the Sierra, notably on the west slope of Miami Mountain, 
about 15 miles east of Mariposa, and near the small settlement 
of Salt Springs, 10 miles farther southeast. 

SALT SPRING NEAR ANTELOPE VALLEY (KERN 1). 

A few saline springs and seepages issue from the marine sediments 
that border the southwest side of San Joaquin Valley. One of them 
is at the edge of the valley, about 4 miles south of the -northern 
border of Kern County and 15 miles northeast of Annette post office. 
The yield of the spring is small, and the water has not been used, 
as it is too saline to be suitable for drinking:. 



SALT SPRINGS NEAR KESSLER ONYX MARBLE QUARRY (SAN LUIS 

OBISPO 11). 

Salt Creek, near Kessler onyx marble quarry, has been mentioned 
in the description of the carbonated springs (p. 164). It is here 
referred to again because of the notable amounts of salt that are 
deposited along its bed and in several other ravines near by. The 
quantity is sufficient to render the stream channels white during 
the summer, and the small amount of water that flows is strongly 
saline. 

The liills of the locality are composed of shales and sandstones 
of probable Tertiary age. The salt is evidently leached from them 
by water that issues as surface springs. 



302 SPEINGS OF CALIFORNIA. 

SALT SPRINGS NORTH OF FURNACE CREEK RANCH (INYO 19). 

The sink or lowest portion of Death Valley, in the eastern part of 
the State, is crusted with impure salt, and at several places along its 
borders small springs issue whose waters are strongly saline. One 
group of springs of this character is situated about 10 miles north 
of the Furnace Creek ^ ranch at the northeast border of Death Valley, 
where a slight amount of salty water issues. 

SALT SPRINGS SOUTH OF FURNACE CREEK RANCH (INYO 21). 

About 4 miles south of the Furnace Creek ranch saline water 
forms a small wet area at the east edge of Death Valley. The flow 
is slight and the water is too salty to be drinkable. 

POISON SPRING (INYO 18). 

Poison Spring is on the western border of Death Valley, 7 miles 
northwest of the Furnace Creek ranch. It yields salty water that 
probably also contains sulphates, whose sickening effect on thirsty 
travelers has given the spring its name. 

VALLEY SPRING (SAN BERNARDINO 2). 

A few strongly saline springs issue in the southern extension of 
Death Valley proper, in the portion that is known as South Death 
VaUey. Valley Spring, which rises in a marshy area on the western 
side of South Death Valley, is probably the largest of these. The 
water forms a clear stream that flows for a short distance, but it is 
strongly saline.^ The source of the water is believed to be Amargosa 
River, which normally sinks a few miles to the southeast. A portion 
of its flow is apparently brought to the surface at the spring by a 
ledge of rock that is there exposed above the valley floor. 

SALT SPRING (SAN BERNARDINO 4). 

Salt Spring, at the southeast end of South Death Valley and about 
5 miles southwest of Dumont railroad station, is probably better 
known than the saline springs farther north in the valley (San Ber- 
nardino 2). It was mentioned many years ago by Fremont, who 
camped there in April, 1844, and described the springs as being "a very 
poor camping ground; a swampy, salty spot, with a little long, un- 
wholesome grass ; and the water which rose in the springs being useful 
only to wet the mouth but entirely too salt to drink." ^ The springs 
are in the canyon of South Branch of Amargosa River. This canyon 

1 The name Furnace was applied to this creek not because of the climate of the region but because a 
small furnace for the reduction of ore was built near its mouth in 1862. 

2 An analysis purporting to represent this water (U. S. Geol. Survey Water-Supply Paper 224, p. 46) is 
believed to be that of water from Owens Lake. 

3 Fremont, J. C, Report of the exploring expedition to the Rocky Mountains, p. 264, 1845. 



SALINE springs'. 303 

forms a pass between the Kingston Range and the Avawatz Moun- 
tains, but desert travel has been mainly north of it, through the 
canyon of the main branch of the river. It has been said that the 
water contains arsenic, as several people have perished from drink- 
ing it, but the fatalities have probably been due rather to the effect 
of such a strong solution of Epsom and Glauber salts on persons who 
were nearly delirious with thirst. 

GARLIC SPRING (SAN BERNARDINO 10). 

There are a few other saline or alkaline springs in the southeastern 
portion of the State that may here be mentioned because of their 
notably mineralized character. One of these is Garlic Spring, which 
is on the road between Daggett and Death Valley, about 35 miles 
northeast of the former place. It yields a small supply and has been 
used as a camping place, but its water contains a large amount of 
sodium, magnesium, and sulphates. 

BITTER SPRING (SAN BERNARDINO 11). 

Bitter Spring is about 12 miles east of Garlic Spring and near the 
southeast side of a small intermittent lake. It formed a watering 
place on the emigrant road between Salt Lake City and San Bernar- 
dino as early as 1852 and has been a camping place since that time, 
but the water contains large amounts of sodium and sulphates. 

DEADMANS HOLES (SAN BERNARDINO 41). 

There are small pools, known as Deadmans Holes, in the playa 
surface at the northwest side of Mesquite Dry Lake, near the road 
between Victorville and Dale mining camp. These pools or springs 
are sometimes used as watering places, but their water contains large 
amounts of alkaline material, probably sodium, magnesium, and 
sulphates. 

SODA SPRINGS (IMPERIAL 3). 

Soda Springs are about 25 miles south of Mecca, on a road along the 
western side of Colorado Desert. They yield, a small amount of 
water that is too strongly saline to be suitable for drinking, but 
travelers are sometimes obliged to use it. 

The springs are situated at the base of a low barren knoll of Ter- 
tiary sediments, and the saline constituents of the water are probably 
obtained directly from these marine deposits. An analysis that is 
given among the carbonated springs under the heading of McCain 
Springs (p. 248) shows the general character of the alkaline saline 
springs of this part of the State. 



304 



SPRINGS OF CALIFOENIA. 



KANE SPRING (IMPERIAL 6). 

Kane Spring issues from a low knoll in a patch of cane and salt 
grass, 2 or 3 miles south of the channel of Carrizo Creek, on the 
southwest side of Salton Sink. Its water is strongly charged Avith 
soda salts. The spring is below sea level and rises in lake sediments 
whose content of alkaline salts has been concentrated at the spring 
by the great evaporation that takes place in this region. 

YUHA SPRING (IMPERIAL 8). 

Yuha Spring is about 20 miles west of El Centro and 2 miles south 
of the road between Imperial Valley and the settlements of eastern 
San Diego County. The water rises in a wash and has little if any 
flow, but in 1905 a pump and a trough furnished means for watering 
horses. The water is notably saline and alkaline, but it is drinkable. 

CASTALIAN MINERAL WATER (INYO 15). 

A few saline waters that are obtained from wells and lakes have 
become known as mineral-spring waters and therefore may be men- 
tioned among the saline springs. 

Analyses of Casialian Mineral Water and water from Owens Lake, Inyo County, Cal. 
[Constituents are in parts per million.] 



Properties of reaction: 

Primary salinity 

Secondary salinity 

Tertiary salinity 

Primary alkalinity 

Secondary alkalinity. . . 
Tertiary alkalinity 



(?) 



56 



44 
Trace. 



(?) 



57 



43 
Trace. 



(?) 



55 



45 
Trace. 



(?), 



54 



46 
Trace. 



Constituents. 



By 

weight. 



Reacting 
values. 



By 
weight. 



Reacting 
values. 



By 
weight. 



React- 
ing 
values. 



weight. 



React- 
ing 
values. 



Sodium (Na), , 

Potassium (K) 

Lithium (Li) 

Rubidium (Rb) and cae- 
sium (Cs) , 

Thorium (Th) , 

Calcium (Ca) , 

Magnesium (Mg) 

Iron(Fe) 

Aluminum ( Al) 

Sulphate (SO4) 

Nitrate (NO3) 

Chloride (01); 

Bromide (Br) and iodide 
(I) 

Sulphide (S) 

Carbonate (CO3) 

Metaborate (BO2) 

Arsenate (AsGi) 

Phosphate (PO4) 

Silica (SiOa) 



29, 300 
1,188 



1,273.5 
30.4 



21,660 

2,750 

Trace. 



941.7 

70.4 

Trace. 



26, 840 
1,548 



1,167.0 
39.6 



Trace. 
Trace. 
Trace. 



Trace. 
Trace. 
Trace. 



Trace. 
Trace. 



Trace. 
Trace. 



7,530 
'26,'26o' 



Traces. 

325 

16, 710 

Trace. 



156.9 



569.7 

Traces. 

20.3 

557.0 

Trace. 



Trace. 

9, 360 

Trace. 

13,440 



Trace. 

194.8 
Trace. 

378.9 



13 
4.7 
9.2 

12 
7,065 



.7 

.4 

.3 

1.3 

147.2 



81, 180 

3,448 

57 

Traces. 

Trace. 
34 
15 



3,530.0 

88.2 
8.2 

Traces. 

Trace. 
1.7 
1.2 



18, 220 



514.0 



21,170 

948 

52,900 



5.3 

440.7 

15.3 

1,492.0 



13, 152 
Trace. 



438.4 
Trace. 



16,500 
190 



549.9 

4.4 



Trace. 
245 



Trace. 
8.1 



Trace. 
164 



Trace. 
5.4 



207 



6.9 



329 
156 
238 
297 



1,667.0 
7.8 
3.4 
7.5 
9.7 



75, 498 



70,608.9 



209, 700 



n Iron and aluminum oxides expressed as aluminum. 



6 Calculated. 



1. Castalian Mineral Water. Analyst, Thomas Price (1880). Authority, U. S. Geol. Survey Bull. 32. 

2. Owens Lake. Analyst, Oscar Loew (1876). Authority, Wheeler report. 

3. Owens Lake. Analyst, T. M. Chatard (1886). Authority, U. S. Geol. Survey Bull. 60. 

4. Owens Lake. Analysts, C. H. Stone and F. M. Eaton. Authority, Am. Chem. Soc. Jour., p. 1169, 
1906. 



SALINE SPRINGS. 



305 



Castalian Mineral Water, which has been sold for medicinal use, 
has been obtained either directly from Owens Lake, in Inyo Coimty, 
or from springs close to its shore. An analysis that is thought to 
represent the bottled water is here tabulated with analyses of water 
from Owens Lake. The analysers on page 304 indicate that the 
waters are similar in character, if not identical, being primary saline 
and alkaline. 

LAKESIDE MINERAL WELLS (SAN DIEGO 12). 

Lakeside Mineral Wells are situated on property belonging to the 
Lakeside Inn, which is 22 miles by railroad northeast of San Diego. 
Three wells that were here sunk about 1906 in the valley of San 
Diego River yield mineralized waters that are known, respectively, 
as Soda, Iron-soda, and Saline. Water from the first two weUs has 
been piped to hydrants in a small house near the inn and is used for 
drinking. The following analysis of the Iron-soda water shows that 
it is primary saline and secondary alkaline in character. The content 
of iron is not unusually high. 

Analysis of ivater from Iron-soda well, Lakeside Mineral Wells, San Diego County, Cal. 

(Analyst, Smith, Emery & Co. (1907). Authority, advertising matter. Constituents are in parts per 

million.] 



Properties of reaction: 

Primary salinity 

Secondary salinity. . , 

Tertiary salinity 

Primary alkalinity. . 
Secondary alkalinity 
Tertiary alkalinity . . 



Constituents. 



By 

■weight. 



React- 
ing 
values. 



Sodium (Na) 

Potassium (K) 

Calcium (Ca) 

Magnesium (Mg) 

Iron(Fe) 

Sulphate (SO4) 

Nitrate (NO3) 

Chloride (CI) 

Carbonate (CO3) 

Phosphate (PO4) 

Silica (Si02) 

Carbon dioxide (CO2) 



190 


8.25 


Trace. 


Trace. 


62 


3.10 


27 


2.22 


2.4 


.09 


78 


1.61 


.6 


.01 


226 


6.38 


169 


5.63 


Trace. 


Trace. 


37 


1.23 



792.0 



A mildly saline water, similar to the Lakeside water, was formerly 
obtained from a well on the grounds of Coronado Hotel, on the sand 
spit or peninsula that forms a protecting arm of San Diego Bay. The 
water had a local sale for table use and was also used at the hotel, 
but an attempt to increase the supply by deepening the well resulted 
in obtaining a strongly saline, unusable water, and the well has long 
been abandoned. 

35657°— wsp 338—15 2n 



306 



SPRINGS OF CALIFORNIA. 



AQUA VITJE MINERAL WELL (LOS ANGELES 13). 

Aqua Vitas Mineral Water is obtained from a well in the north- 
eastern part of the city of Los Angeles. The well is about 400 feet 
deep and the mineralized water rises to within about 40 feet of the 
surface. The water, which is pumped into cement reservoirs and 
thence piped to an adjacent bottling house, has been on the local 
market since 1901 or 1902 and has been sold both natural and car- 
bonated. The following analyses show that the water is primary 
and secondary saline in character. These analyses were made sev- 
eral years apart and indicate a considerable change in the character 
of the water that is probably accounted for largely by the decay of 
the casing and admission of other than the lower mineralized water 
into the well. 



Analyses of Aqua Vitse Mineral Water, Los Angeles County, Cal. 
[Authority, advertising matter. Constituents are in parts per million.] 



Properties of reaction: 

Primary salinity 

Secondary salinity . . . 

Tertiary salinity 

Primary alkalinity. . . 
Secondary alkalinity . 
Tertiary alkalinity. . . 



Constituents. 



By 
weight. 



Sodium (Na) 

Calcium (Ca) 

Magnesium (Mg). 

Iron(Fe).... 

Sulphate (SO4)... 

Chloride (01) 

Carbonate (CO3). 
Silica (Si02) 



399 
264 



20 
1,174 



145 
20 



2,091 



Carbon dioxide (CO2) . 



Reacting 
values. 



By 
weight. 



17.36 
13.17 



232 
252 
109 



.71 

24.45 

1.95 



876 
91 

325 
36 



1,921 



178 



Reacting 
values. 



10.09 
12.58 
8.97 



18.24 
2.57 

10.83 
1.19 



8.09 



1. Analysts, Childs and Hansen, several years prior to 1909. 

2. Analyst not given; made in 1909. 

SAN BENITO MINERAL WELL (SAN BENITO 1). 

San Benito Mineral Water has been obtained for a number of years 
from Mr. A. F. Anderson's well, about 4 miles southeast of HolHster, 
in San Benito County, and has been carbonated and bottled by the 
local soda works. The following analysis shows that the water is 
rather concentrated and is primary saline in character: 



SALINE SPKINOS. 



307 



Analysis of San Benito Mineral Water, San Benito Countij, Cal. 
[Analyst, M. E. Jaffa. Authority, 13th Cal. Con.stituents are in parts per million.] 




Properties of reaction: 

Primary salinity 

SepoTidary salinity 

Tertiary "salinity 

Primary alkalinity 

Secondary alkalinity 

Tertiary alkalinity 

Constituents. 

Sodium (Na) 

Potassium ( K) 

Calcium (Ca) 

Magnesium (Mg) 

Iron(Fe) 

Sulphate (SO,) 

Chloride (CI) 

Carbonate (CO3) 

Silica (Si02), organic matter, and combined water 



Tlie well was put down in the early nineties. Water was first struck 
at a depth of 100 feet, and drilling was stopped at 167 feet in blue clay, 
but a sufficient supply of water was not obtained and the well was 
deepened a year later. The minerahzed water was struck at a depth 
of 286 feet, where drilling was discontinued. The water stands about 
100 feet below the surface and is pumped by a windmill for domestic 
use. Its strongly sulphated character renders it laxative and pre- 
vents its free use for drinking at first, but those who use it daily 
gradually become accustomed to it and it ceases to have notably 
medicinal efi^ect. 

Clays and coarser sediments of Tertiary age form low rolUng hills 
that border San Benito Valley in this locality. The mineral con- 
stituents of the water are evidently derived from these marine 
sediments. 

TAMALPAIS MINERAL WELL (MARIN 2). 

Tamalpais Mineral Well is situated in the town of San Rafael, in 
Marin County. A mildly saline water that is obtained from it has 
been carbonated and bottled for a number of years as Tamalpais Nat- 
ural Mineral Water and is also used with sirups in the preparation of 
carbonated beverages. The well is in the southern part of the town, 
at the base of a tuffaceous hill, and has been sometimes referred to as 
San Rafael Spring. The water rises in a stone-curbed well 6 feet in 
diameter and 25 feet deep in the basement of the building of the 
Buffalo Soda Works. 



308 



SPRINGS OF CALIFOKlSriA. 



The following analysis shows it to be a secondary alkaline and 
primary saline water: 

Partial analysis of Tamalpais Natural Mineral Water, Marin County, Cal. 
[Analyst, Price & Son. Authority, owner of well. Constituents are in parts per million.] 



Properties of reaction: 

Primary salinity 

Secondary salinity. . . 

Tertiary salinity 

Primary alkalinity... 
Secondary alkalinity . 
Tertiary "alkalinity .". . 



(?) 



33 

Small. 



67 



Constituents. 



weight. 



Reacting 
values. 



Sodium (Na) 

Calcium (Ca) 

Magnesium (Mg). 
Sulphate (SO4).-. 

Chloride (CI) 

Carbonate (CO3). 



79 

138 

Small. 
121 
207 



3.42 

6.90 

Small. 
3.42 
6.90 



HUMBOLDT ARTESIAN MINERAL WELL (HUMBOLDT 2). 

Humboldt Mineral Water was carbonated and bottled for many 
years as a table water. The following analysis indicates that the 
water is secondary alkaline and primary saline in character: 

Analysis of Humboldt Mineral Water, Humboldt County, Cal. 
[Analyst, W. D. Johnson (1894?). -Authority, 12th Cal. Constituent's are in parts per million.] 



Properties of reaction: 

Primary salinity 

Secondary salinity . . . 

Tertiary salinity 

Primary alkalinity. . . 
Secondary alkalinity. 
Tertiary alkalinity . . . 



Constituents 



(?) 



By 

weight. 



Reacting 
values. 



Sodium (Na) 

Calcium (Ca) 

Magnesium (Mg). 

Iron (Fe) 

Aluminum (Al).. 
Sulphate (SO4)... 

Chloride (CI) 

Carbonate (CO3). 
SUica(Si02) 



Carbon dioxide (CO2). 



200 
94 

44 

.6 

1.7 

Trace. 

285 

268 

19 



8.70 

4.67 

3.59 

.02 

.17 

Trace. 

8.04 

8.92 

.62 



912.3 



Excess. 



The water was obtained from the Humboldt Artesian Mineral Well, 
which is situated near the edge of the bay, at high-tide level, about a 
mile south of Eureka, and is now within the boiler room of Flanna- 
gan's lumber mill. The well is 6 inches in diameter and 1 75 feet deep, 



MAGNESIC SPRINGS. 309 

and water is pumped from it to supply the water boxes of the lumber 
company. The pump is run constantly during working hours and 
lifts 30,000 gallons a day, but 5 minutes after pumping is stopped the 
well overflows. Much gas rises with the water, and in order to 
prevent its interference with pumping the well has been capped and 
a 2|-inch pipe extends down the well a considerable distance. 

The well is sunk into the alluvium and more consolidated sediments 
that border the bay, and its water evidently obtains its saline and 
other constituents directly from the marine beds. 

MAGNESIC SPRINGS. 

SPRINGS PREVIOUSLY DESCRIBED. 

Most of the magnesic springs in the State have been described 
under headings suggested by other more pronounced characteristics, 
but it has been thought advisable to give them brief mention under 
one heading. The. springs at Duncan (Mendocino 31 , p. 167), Howard 
(Lake 51, p. 95), Spiers (Lake 52, p. 190), Napa Rock (Napa 9, p. 161), 
and Phillips (Napa 8, p. 161) springs and at The Geysers (Sonoma 4, 
p. 83), as has already been noted, issue from serpentinous rock from 
which they evidently derive their magnesium contents. A few other 
springs contain large amounts of magnesium that is apparently 
derived from sources other than serpentine. Several of the desert 
alkaline springs are of this character, but perhaps the most notable 
are Alhambra Springs (Contra Costa 2, p. 293) and the group near 
Santa Barbara, including Veronica Springs (Santa Barbara 3, p. 294). 
These waters contain large amounts of magnesium, which is probably 
derived from ocean water, although it has been concentrated by some 
process that is not clearly understood. 

MENDENHALL SPRINGS (ALAMEDA 6). 

Mendenhall Springs are 1 1 miles by road southeast of Livermore 
on the steep southwestern side of the canyon of AiToyo Mocho, 
500 feet above the stream. Two springs here seep from short pros- 
pect turmels 50 yards apart that were driven many years ago in search 
of gold. The water was early noticed to be perceptibly mineraUzed, 
the perceptible taste apparently being due to magnesia, and a number 
of years ago it was bottled as Agua de Vida (Water of Life) Springs 
Water. 

The water of the southern spring is piped to a tank and furnishes 
a domestic supply; the other spring suppUes a watering trough in 
the barnyard. Their flows are respectively about 1 gallon and 
half a gallon a minute. 



310 



SPRINGS or CALIFOENIA. 



The following analyses show that they are essentially primary saline 
and secondary alkaline waters, the upper spring having the higher 
salinity: 

Analyses of water from Mendenhall Springs, Alameda County, Cal. 
[Constituents are in parts per million.] 



Temperature 

Properties of reaction: 

Primary salinity 

Secondary salinity . . . 

Tertiary salinity 

Primary alkalinity . . . 
Secondary alkalinity. 
Tertiary alkalinity. . . 



(?) 



U°C.(58°F.). 

42 
18 


40 
32 



Constituents. 



By 

weiglit. 



Sodium (Na) 

Potassium (K)... 

Calcium (Ca) 

Magnesium (Mg). 
Aluminum (Al).. 
Manganese (Mn). 
Sulphate (SO4)... 

Chloride (CI) 

Carbonate (CO3) . 
Silica (Si02) 



136 

5.5 
95 
41 

3.3 



178 
42 
278 
7.2 



786. 



Carbon dioxide (CO2) 

Hydrogen sulphide (H2S) . 



164 



Reacting 
values. 



By 

weight. 



5.91 

.14 

4.72 

3.36 

.37 



106 

44 



3.70 

1.18 

9.25 

.24 



144 
38 
270 
7.2 



705.2 



Present. 



Reacting 
values. 



By 

weight. 



5.30 
3.61 



3.00 
1.08 
8.99 
.24 



148 

Trace. 

104 

46 

3.6 

Trace. 

374 

52 

183 

9.4 



920.0 



Reacting 
values. 



6.43 

Trace. 

5.17 

3.77 

.40 

Trace. 

7.78 

1.48 

6.11 

.32 



3.58 
1.06 



1. Lower Spring. Analyst and authority, Winslow Anderson (1888). 

2. Lower Spring. Analyst, Falkenau and Reese. Authority, 8th Cal. 
3.. Upper Spring. Analyst and authority, Winslow Anderson (1889). 

The water is apparently of surface origin and has become some- 
what minerahzed from the materials through which it percolates. 
The tunnels are driven into thin-bedded cherts and crushed shales 
that belong to the Franciscan group. 

The property has been improved as a mountain resort for a num- 
ber of years. In 1909 accommodations for 75 people were provided 
by several cottages and by a dining room in the main building. 

SWEET SPRINGS (ALAMEDA 6). 

Another group of magnesic springs that are associated with ser- 
pentinous rock rise at the border of a small meadow on a low saddle 
between two ravines 18 miles southeast of Livermore. The group, 
which is known as Sweet Springs, includes 10 that issue for a space 
of 200 yards along the southern side of the meadow and 4 others that 
issue on its eastern side. They range in size from mere seepages to 
flows of 6 or 8 gallons a minute, the total yield being perhaps 30 
gallons a minute. The water has a distinctly sweet taste. The 
locality has been used by range stock as a watering place. 



MAGNESIC SPRINGS. 311 

The principal springs rise from the northern border of an area of 
pyroxene rock and serpentine which cover the slopes to the south, 
the slopes nortli of the springs being of siliceous sandstone. The sand- 
stone probably belongs to the Franciscan group of altered sediments, 
which occupies considerable areas in the Coast Ranges, and the 
serpentine bears its usual intrusive relation to the sediments. 

ISHAM SPRING (SAN DIEGO 15). 

In the granitic ranges northeast of San Diego there are a number 
of small springs whose waters have been developed commercially for 
table and medicinal use. Isham Spring is probably the best known 
of these, as its water has been on the market for many years. It was 
formerly known locally as Baldhead Spring, as the use of its water 
was thought to aid in preventing baldness. The spring is situated in 
a swale near the head of a small tributary of Sweetwater Kiver, 12 
miles by road north of east from San Diego. The water issues in a 
small cemented and inclosed basin at the side of the drainage channel, 
from two crevices in the bedrock. It is piped thence to a small reser- 
voir and to a bottling house. 

The water is noticeably mineralized, magnesia apparently being 
the constituent most evident to the taste, and the analysis, which 
is tabulated on page 312 with that of another commercially developed 
spring in the same locality, shows that the water is primary and sec- 
ondary saline and secondary alkaline in character. 

The rock of the locality is considerably decomposed and evidently 
furnishes the main soluble constituents of the water. A small amount 
of lune carbonate has been deposited along the side of the ravine near 
the spring and also on the hillside a few hundred yards eastward. 

NUVIDA SPRING (SAN DIEGO 16). 

Nuvida Spring is a few miles southeast of Isham Spring, being 8 
mdes by road from La Presa railroad station. Its water has been 
placed on the market for table and medicinal use. The following 
analysis shows that it is essentially secondary saline in character, 
with magnesia fairly well represented though not very noticeable to 
the taste. 



312 



SPRINGS OF CALIFORNIA. 



Analyses of water from Isham and Nuvida springs, San Diego County, Cal. 
[Authority, advertising matter. Constituents are in pai'ts per million.] 



Properties of reaction: 

Primary salinity 

Secondary salinity 

Tertiary salinity 

Primary alkalinity 

Secondary alkalinity 

Tertiary alkalinity 

Constituents. 

Sodium (Na) 

Potassium (K) 

Calcium (Ca) 

Magnesium (Mg) 

Iron ( Fe) 

Aluminum (Al) 

Manganese (Mn) 

Sulphate (S0<) 

Chloride (CI) 

Bromide (Br) 

Iodide (I) 

Carbonate (CO3) 

Arsenate (AsOd) 

Phosphate (P0<) 

Silica (Si02) 



By 
weight. 



Reacting 
values. 



By 
weight. 



Reacting 
values. 



110 

18 
95 
57 



1.4 

52 

346 

Trace. 

.1 

117 

Trace. 

Trace. 

S3 



4.78 

.45 

4.73 

4.71 

.01 

.09 

.05 

1.08 

9.76 

Trace. 

Trace. 

3.89 

Trace. 

Trace. 

1.76 



19 

Trace. 

139 

108 

2.0 

7.9 

20 

55 

454 



Trace. 

6.93 

8.91 

.07 

.87 

.73 

1.15 

12.79 



9.1 

104 



.07 
3.47 



102 



850.6 



1,020.0 



1. Isham Spring. Analysts, Price & Son. 

2. Nuvida Spring. Analyst, C. E. Munroe. 

IRON SPRINGS. 

SPRINGS PREVIOUSLY BESCRIBED. 

A few of the springs of California deserve separate consideration 
because of the exceptionally large quantities of iron deposited by 
their waters. Among those that have already been described prob- 
ably the most noteworthy in this respect are Arlington Springs 
(Plumas 12, p. 229), which have been mentioned among the carbonated 
springs, though they might as properly be described as iron springs^ 
for their waters have deposited so much of the mineral that the sur- 
rounding soil has been used locally as an ocher for the preparation of 
paint. 

IRON SPRINGS IN YOSEMITE VALLEY (MARIPOSA 4). 

Probably one of the most frequently visited groups of iron springs 
in the State is half a mile southwest of MuTor Lake in Yosemite 
Valley, on the western side of the outlet of the lake. Two springs 
rise at this place. At the lower one the water issues around the edge 
of an oval depression a few yards in diameter, 2 or 3 feet below the 
normal surface of the valley soil. A keg that has been sunk near the 
center of the depression forms a drinking pool which yields about 
10 gallons a minute of cold excellent water. The second spring rises 
about 50 yards farther upstream, in an area of marshy ground a few 



ARTESIAN SPRINGS. 313 

yards iii diameter. Its immediate yield is perhaps 15 gallons a 
minute, but this is increased by other seepages, so that the combined 
flow of the two si)rings and the seepages forms a stream of perhaps 
30 gallons a minute. Much soft brown deposit along the course of 
the overflow and m the marshy land possibly consists to large extent 
of Crenothrix, a vegetable organism that secretes iron. 

IRON SPRINGS NEAR LAKE TAHOE (PLACER 12). 

A mile northwest of McKmney, on the western side of Lake Tahoe, 
two small iron springs rise in the woods on a gentle slope about 350 
yards above the main wagon road and form pools about a foot in 
diameter and a foot in depth, 4 yards apart, which are used for 
drinkmg. The water tastes distinctly ferruginous and has deeply 
iron stained the soil for about 75 yards below the springs. The 
staining is probably caused by the fact that the water contains a 
small amoimt of carbon dioxide, which holds the iron in solution until 
this gas has escaped, when the iron is precipitated and deposited 
along the overflow course. 

The springs issue from lake deposits of sand and gravel near the 
base of steep slopes of andesitic lava. 

IRON SPRING NEAR CISCO (PLACER 1). 

A cold iron spring that yields perhaps 8 gallons a minute is situated 
in a small depression in a patch of alders on a gentle slope on the 
southern side of the canyon of South Fork of Yuba River, half a mile 
north of Cisco railroad station and 100 yards south of the wagon 
road. The soil is deeply iron stained for a number of yards along 
the overflow channel. The spring is well known locally, as it fur- 
nishes excellent cold drinking water. The surrounding rocks are 
the slates and schists derived from them that have been mentioned 
in speaking of the sulphur springs near South Fork of Yuba River 
(Placer 2, p. 284), a mile or two upstream from the iron spring. 

ARTESIAN SPRINGS. 

SPRINGS PREVIOUSLY DESCRIBED. 

Many of the springs that rise in the alluvial valleys of the State 
yield considerable good water that is noticeably above a normal tem- 
perature and that is apparently forced to the surface through the 
deep alluvial deposits by artesian pressure. Several springs in 
Sonoma County, notably those on McEwan ranch (Sonoma 14, p. 
114), Los Guilicos Warm Springs (Sonoma 15, p. 114), and the Warm 
Springs of the State Home at Eldridge (Sonoma 16, p. 114), which 
have been described among thermal springs, may also be mentioned 
in connection with artesian springs, as they rise in tufFaceous lava, 



314 SPRINGS OF CALIFORNIA. 

the structure of which is apparently adapted to carry and yield 
water under artesian pressure. The artesian wells at Agua Caliente, 
Fetters, and Boyes hot springs (Sonoma IS, 19, and 20, pp. 112-114) 
also furnish evidence in support of the theory that the natural warm 
springs are of artesian origin. Boyd Spring (Modoc 12, p. 124) has 
characteristics which suggest that it is supplied by alluvial artesian 
water, but the fact that all the other notable springs in Surprise 
Valley are too hot to be of artesian origin favors the opinion that the 
source of Boyd Spring also is deep-seated, its water rising along a 
structural break. 

The warm springs at south end of Surprise Valley (Modoc 18, 
p. 124), like Boyd Spring, may possibly be supplied by alluvial artesian 
water, but a more probable source is heated water that may rise along 
a fault or structural break. 

TORO SPRINGS (RIVERSIDE 14). 

Near the northern end of Salton Sink in the Colorado Desert the 
artesian water that underlies this portion of the desert rises to the 
surf ace, forming several ''cienagas" or marshy areas. The northern- 
most of these cienagas that is worthy of note is at Toro Springs, on 
the Toro Indian Reservation, about 9 miles south of Indio. There 
has been an Indian settlement at the springs for many years, and the 
water has been used by the Indians to irrigate garden patches. 

ALAMO BONITO SPRINGS (RIVERSIDE 15). 

Alamo Bonito Springs are about 5 miles southwest of Mecca and 8 
miles southeast of the Toro Springs, to which they are similar. The 
name, which is Spanish and means "beautiful poplar," refers to the 
trees that are numerous in the vicinity of the springs. Like Toro 
Springs there has been an Indian settlement at them for many years. 

AGUA DULCE SPRINGS (RIVERSIDE 16). 

Agua Dulce (sweet water) Springs are about 7 miles south of Mecca 
and were close to the margin of Salton Sea at its highest stage in 1907. 
Several springs in the group have long been used by the Indians. 
They were formerly an important watering place on the road along 
the western side of the desert, but within recent years their value 
has been lessened by the fact that other supplies of water have been 
obtained from a number of flowing wells in the neighborhood. 

FIGTREE JOHNS SPRINGS (RIVERSIDE 17). 

A small group of springs about 3 miles southeast of Agua Dulce 
Springs has long been known by the name of an Indian, Figtree John, 
who, with his family, has lived near the springs and cultivated a small 
garden and orchard. In 1907 the springs were submerged to a depth 



ARTESIAN SPRINGS. 



315 



of a few feet by the rising; wator of Saltoii Sea, but they have doubtless 
been exposed again as the kn'cl of the sea has been lowered. 

FISH SPRINGS (IMPERIAL 1). 

Fish Springs, which are about 3 miles southeast of those of Figtree 
John, were submerged to a depth of about 25 feet in 1907 by the 
water of Salton Sea. They yielded a considerable flow of tepid, 
slightly saline water and formerly constituted an important watering 
place on the western side of the desert, for they furnished the southern- 
most potable water for a number of miles. They will again be of 
value to travelers when they are exposed by the subsidence of the 
lake water. 

DOS PALMAS SPRINGS (RIVERSIDE 18). 

A group of tepid, rather salty springs that seem to be of artesian 
origin is situated about 6 miles east of Salton railroad station, on the 
northeastern side of Salton Sink. The locahty was formerly a well- 
known camping place on the road between San Bernardino and Yuma, 
but it has not been much used for this purpose since the construction 
of the railroad through the region. The following analysis of the 
water of the springs shows that it is primary and secondary saline in 
character: 

Analysis of ivater from wMin spring, Dos Palmas Springs, Riverside County, Cal. 
[Analyst, Oscar Loew (1870). Authority, Wheeler report. Constituents are in parts per million.] 



Properties of reaction: 

Primary salinity 

Secondary salinity 

Tertiary salinity 

Primary alkalinity 

Secondary alkalinity 

Tertiary alkalinity 

Constituents 

Sodimn (Na) 

Calcium (Ca) 

Magnesium ( Mg) 

Manganese ( Mn) 

Sulphate (SOi) 

Chloride (01) 

Carbonate (CO3) 

Phosphate (PO4) 

Silica (SiOz) 



(?) 



20 



Trace. 



By 
weight. 



Reacting 
values. 



96 

63 

Trace. 

477 

1,400 

Trace. 

Trace. 

Trace. 



2,944 



39.50 

4.79 

5. 15 

Trace. 

9.94 

39.50 

Trace. 

Trace. 

Trace. 



OROCOPIA SPRINGS (RIVERSIDE 19). 

Orocopia Springs, which are half a mile east of Dos Palmas Springs, 
rise in a marshy area several acres in extent. A plentiful supply 
of mildly saline water is obtained from several large holes cut in the 
sod. The Orocopia Mining Co, has established a pumping plant at 



316 SPEINGS OF CALIFOElSriA. 

the springs, and the water is pumped to the mine, several miles 
northward. 

TWENTY-NINE PALMS SPRINGS (SAN BERNARDINO 44). 

In the region north of the Colorado Desert there are a number of 
springs and groups of springs that are probably supplied by alluvial 
artesian water. Twenty-nine Palms Springs, which form a camping 
place for prospectors and also furnish a water supply for mining 
camps in the near-by mountains, are scattered for a mile along the 
southwest edge of a dry lake, about 45 miles by road northward from 
Indio. They receive their name from groups of palm trees that grow 
near them. 

OLD WOMAN SPRINGS (SAN BERNARDINO 27). 

On the southern border of Mohave Desert, about 4Q miles by road 
south of east from Victorville, two springs issue from the northern 
base of a hill of basic lava. The larger spring, which is known as Old 
Woman Spring proper, flows from a 30-foot tunnel in the hillside. 
In June, 1910, it yielded about 150 gallons a minute, but its flow is 
said to vary considerably with the season. The water is collected in 
an earthen reservoir and is thence used to irrigate an alfalfa field. 
The second spring, which is known as Ponuner Spring, issues from a 
hole beneath a cottonwood tree about 50 yards northwest of the 
main spring. It yields about 12 gallons a minute of water that has 
been used to irrigate an orchard near by. 

COTTONWOOD SPRING (SAN BERNARDINO 26). 

Cottonwood Spring, wliich is 1 mile northwest of Old Woman 
Springs, issues from a 50-foot tunnel in coarse gravel or conglomerate 
near lava slopes. It yields about 3 gallons a minute of water that is 
collected in a small reservoir and used to irrigate a garden. 

The three springs last described — Old Woman, Pommer, and Cot- 
tonwood — are apparently situated at places where alluvial water 
from the slopes of San Bernardino Mountains, which lie to the south, 
is forced to the surface by rock obstruction. In this respect they are 
thought to be similar in origin to Newberry Spring, described on 
page 317. The waters of all three are slightly alkaline, 

RABBIT SPRINGS (SAN BERNARDINO 25). 

Rabbit Springs, which are situated about 25 miles east of Victor- 
vUle, issue from a marshy bank near a group of cottonwood trees. 
The group includes two principal springs, one of which slightly over- 
flows from a box-curbed pool and is used by campers and travelers; 



ARTESIAN SPRINGS. 



317 



the other spring is a quurtor of a mile farther westward and yields 
about 1 gallon a minute, which supplies a cattle trough. Since well 
water has been obtained at the Box S ranch, a mile to the southeast, 
the springs have not been so much used, for the water at the ranch is 
of better quality. 

NEWBERRY SPRING (SAN BERNARDINO 20). 

Newberry Spring rises at the north base of hiUs of tuffaceous lava 
that border a desert flat 600 yards south of Newberry pumping 
station, on the Santa Fe Railway. The spring is surrounded by a 
circular masonry reservoir about 20 feet in diameter, from which an 
8-inch pipe line leads to the pumping station at the railroad. The 
water is used for locomotive supply at this station and is also hauled 
in tank cars for railroad supply at Ludlow and Bagdad, two stations 
farther east. The water is of good quality for boiler use, the follow- 
ing partial analysis showing its character for this purpose : 

Partial analysis of ivater from Newberry Spring, San Bernardino County, Cat. 
[Analyst and authority, Atchison, Topeka & Santa Fe Railway Co. Constituents are in parts per mlllion.J 



Propert ies of react ion : 

Primary salinity 


Present. 


Secondary salinity 





Tertiary salinity.. 





Primary alkalinity 


Present. 


Secondary alkalinity 


About 30 


Tertiary "alkalinity 


(?) 






Constituents. 


By weight. 


Temporary hardness 


91 


Permanent hardness 





Dissolved solids 


324 







The temperature of the water, 77°, indicates that it is of essentially 
alluvial artesian origin, although tlie position of the spring at the 
north base of Kane Mountain suggests that it may be related to 
faulting that probably has taken place here. There are a few mesquite 
trees at the spring, which has long formed a camping place for desert 
travelers. 

BIJCKHORN SPRINGS (KERN 26). 

Buckliorn Springs form a group on the west side of Rodriguez 
Dry Lake and about 7 mUes south of Muroc railroad station. The 
springs rise in low grassy mounds in the lake flat and yield small 
quantities of slightly alkaline water, forming a watering place that 
has been used for many years by prospectors. The cabin of a pros- 
pector has stood near the principal spring for several years and marked 
its location. Several springs of similar character rise at other points 



318 SPEINGS OF CALIFORNIA. 

around the border of this dry lake. All appear to be supplied by the 
upward leakage of alluvial artesian water. ^ 

INDIAN SPRING (KERN 25). 

Indian Spring is situated near the northern border of Rosamond 
Dry Lake, 3 miles east of the station of the same name on the South- 
ern Pacific Railroad, about 200 yards south of the base of steep hills. 
The spring, which has only a slight flow, has been curbed to form a 
cattle-watering pool about 12 feet square, and deeply worn trails 
lead to it. A small box-curbed pool in the center furnishes a water 
supply to prospectors and travelers. The property has been filed 
upon and two or three cabins have been built near the spring. An- 
other spring of similar character but of only seeping flow issues near 
the southern border of the valley, about 13 mfles southward or 2 
miles southwest of the town of Lancaster. 

WILLOW SPRINGS (KERN 22). 

Willow Springs are on the ranch of Mr. E. M. Hamilton, at the 
northern border of Antelope Valley, 8 miles west of Rosamond. 
The ranch forms a small settlement where supplies and accommoda- 
tions for the night may be obtained. 

Several springs and seepages issue for a distance of a quarter of a 
mile along the base of hills that border the valley, and farther west- 
ward, beyond the Willow Springs group, others of similar character 
issue, the principal one being known as Bean Spring. 

In the Willow Springs group 7 springs may be recognized, of 
which the southernmost yields much the greatest supply, its dis- 
charge being (in July, 1909) 15 or 20 gallons a minute. It rises in 
a bricked and cemented chamber, about 15 feet in diameter and 10 
feet high, that has been constructed in an excavation in the bank. 
The water is piped to a cement reservoir about 50 feet in diameter 
and 6 feet deep and is used for irrigation. Water from two or three 
of the other springs is collected in a smaller reservoir and is also 
used for irrigation. About 35 acres of vegetables, alfalfa, and 
orchard are watered by these springs. The following analysis of 
water from the main spring shows it to be a primary saline secondary 
alkaline water of low concentration. 

1 The origin of these springs is discussed by H. R. Johnson, in Water resources of Antelope Valley, 
Calitomia: U. S. Geol. Survey Water-Supply Paper 278, pp. 47^8, 1911. 



ARTESIAN SPRINGS. 



319 



Analysis of water from main springs, Willow Springs, Kern County, Cal. 

[Analyst, Walton Van Wmkle (1909). Authority, U. S. Geol. Survey Water-Supply Paper 278. (Constit- 
uents are in parts per. million.] 



Properties of reaction: 

Primary salinity 

Secondary salinity 

Tertiary salinity 

Primary alkalinity 

Secondary alkalinity 

Tertiary "alkalinity 

Constituents 

Sodium (Na) 

Potassium (K) 

Calcium (Ca) 

Magnesium (Mg) 

Iron ( Fe) 

Aluminum (Al) 

Sulphate (SO<) 

Chloride (CI) 

Carbonate (CO3) 

SiUca(Si02) 

Carbon dioxide (CO2) 



(?) 



By 
weight. 



101 
19 

76 
25 



328.3 



Reacting 
values. 



2.35 

2.20 
.75 

.01 

2.10 

.54 
2.54 



The water issues along a terrace-like bank whose position indicates 
that it may be a small fault. The springs may therefore be supplied by 
alluvial artesian water that here escapes upward along the faulted 



zone. 



RESTING SPRINGS (INYO 34). 



Resting Springs rise at the southern end of a mountain range, about 
5 miles east of the Tonopah & Tidewater Railroad, in southeastern 
Inyo County. Fremont camped at them in 1844, when returning 
eastward from his exploring expedition, and they early became a 
stopping place on the road between Salt Lake City and San Bernar- 
dino. They are still well known to desert travelers, and Mr. Philander 
Lee, who has lived there since 1882, has made a real oasis of the place. 
About 25 acres of alfalfa, corn, and garden vegetables are irrigated 
by the main spring, which is said to yield 29 miner's inches (260 gal- 
lons a minute).^ The springs are situated in a small marshy area at 
the base of a terrace-like bank, 25 yards south of the steep slope of 
Resting Springs Mountain. The water rises in this marshy area 
mainly at four points around the edge of a natural basin about 8 yards 
in diameter, which is sunk several feet below the normal surface. 
The temperature of the water (80°) and its constant flow indicate that 
it is essentially of deep-seated or artesian character, but the mountain 
slope at whose base it issues is composed of quartzite that dips 

1 For discussion of these springs, with diagrams, see Johnson, H. R., Water resources of Antelope Valley, 
California: U. S. Geol. Survey Water-Supply Paper 278, pp. 49-51, 1911. 

The old California miner's inch is approximately equivalent to a flow of 9 gallons a minute. 



320 SPRINGS or CALIFOENIA. 

60° NE,, and the rise of the water may be determined largely by a 
fault along the western face of the ridge. About 200 yards west of 
the main springs a flow of perhaps half a gallon a minute has been 
developed in a small bank and piped to a watering trough beside the 
road. 

Considerable agricultural land extends southwestward from the 
springs, but the higher land eastward and the slopes to the west are 
composed largely of barren knolls and dry washes. 

TEXAS SPRINGS (INYO 20). 

A large amount of slightly saline water rises in Texas Springs, near 
the mouth of Furnace Creek, at the northeast edge of Death Valley. 
The water has been used for irrigation on Furnace Creek ranch for 
a number of years, and the springs have long formed a camping place 
for desert travelers. The water apparently has an alluvial artesian 
source, though it may be related to the rock structure along the 
eastern side of Death Valley. 

BLACKBOCK SPRING (INYO 8). 

Several large springs that rise along the western side of Owens 
Valley are probably supplied by alluvial artesian water, which is 
apparently forced to the surface by lava of relatively recent geologic 
age that has flowed down into the valley from craters near by. Black- 
rock Spring, which is the southernmost and largest, is 10 miles by 
road north of Independence. The water rises in a pool 10 or 15 yards 
in diameter, at the southern base of a low lava ridge, and flows east- 
ward across the flat alluvial valley. The water has been used for 
irrigating meadowland, but it is now a portion of the supply for the 
Los Angeles aqueduct.^ Its temperature (56°) is said to be the same 
as the mean annual temperature that is indicated by records covering 
a period of 12 years at Independence. The normal flow of the spring 
has been measured as 21 second-feet ^ (9,425 gallons a minute), 
but it is said to decrease notably when the water level is raised by an 
irrigation head gate. The following three analyses show wide varia- 
tions in the apparent proportions of certain constituents but in general 
indicate that the water contains little mineral matter in solution: 

1 A gravity canal that conveys the water of Owens River 250 miles southward as a municipal supply for 
the city of Los Angeles. 

2 Second-foot = 1 cubic foot a second. It is the unit that is commonly employed in measuring the dis- 
charge of streams. 



ARTESIAN SPRINGS. 



321 



Analyses of water front. Blarkrock Spring, Inyo County, Cal. 
[Authority, records of Los Ans^eles atiueduct. Constituents are in parts i)er million.] 



Properties of reaction: 

Primary salinity 

Secondary salinity. . . 

Tertiary salinity 

Primal y alkalinity... 
Secondary alkalinity. 
Tertiary alkalinity ". . 



Constituents. 



By 
weight. 



Reacting 
values. 



By 

weight. 



Reacting 
values. 



3 



By 

weight. 



Reacting 
values. 



Sodium (Na) 

Potassium (K)... 

Calcium (Ca) 

Magnesium (Mg). 

Iron(Fe) 

Aluminum (Al).. 
Sulphate (SOi)... 

Chloride (CI) 

Carbonate (CO3). 
Silica (Si02) 



36 



1.55 



7.2 
3.0 

3.0 

21 

7.8 
45 

7.0 



.36 

.24 

.11 

.44 
.22 
1.49 
.23 



9.3 
Trace. 
20 
5.4 

Trace. 

20 

8.3 
37 

6.8 



.40 

Trace. 

1.04 

.45 

Trace. 

.42 
.23 
1.24 
.23 



II 
Trace. 



.46 
Trace. 

.90 



.83 
.05 
.48 
1.00 



130.0 



106.8 



1. Analyst, L. J. Stabler (1906). 

2. Analyst, G. E. Col!>y (1905). 

3. AnalS^st, Wade & Wade (1905). 

LITTLE BLACKROCK SPRING (INYO 7). 

Little Blackrock Spring, which rises at the valley edge half a mile 
west of north from Blackrock Spring, forms a pool a few yards in 
diameter at the edge of a lava flow and also forms part of the supply 
for the Los Angeles aqueduct. Its normal discharge is about 7 sec- 
ond-feet (3,140 gallons a minute), but its flow is said to increase when 
that of Blackrock Spring is decreased by the closing of an irrigation 
head gate. 

HINES SPRING (INYO 5). 

Hines Spring rises in a marshy and tule-grown area at the southern 
base of a lava ridge 8 or 10 feet high that is 3 J miles north of Black- 
rock Spring. Its water had not been made use of when the spring 
was visited in 1908, and it formed a sluggish stream about 3 feet wide. 

SEELYS SPRING (INYO 4). 

Seelys Spring is about 2 J miles north of Hines Spring. It rises at the 
south base of a low lava ridge 75 yards from the west bank of Owens 
River, into which it flows directly. It yields IJ second-feet (600 
gallons a minute)^ of good water that has a temperature of 61°. 

• Measurement made with current meter Nov. 15, 1908, by A. T. Barrows, jr. 
35657°— wsp 338—15 21 . 



322 SPEINGS OF CALIFORNIA. 

FISH SPRINGS (INYO 3). 

Fish Springs are at the west edge of Owens Valley, about 3^ miles 
south of Big Pine or 27 miles north of Independence. They form a 
large pond at the northern side of a lava ridge that extends for some 
distance into the valley. The water has not been efficiently used, 
but it irrigates a small amount of meadow along its course eastward 
to Owens River. 

DEEP SPRINGS (INYO 2). 

At the southern end of Deep Spring Valley, in the northeastern 
part of Inyo County, are several large artesian springs that have been 
used for a number of years for irrigation, and their supply is said to 
be sufficient to water 600 acres. The springs are about 18 miles by 
road northeast of Alvord railroad station and form a stopping place 
on the road to Nevada. The largest group of springs is sometimes 
known as Buckhorn Springs. Water issues at numerous places, how- 
ever, for a distance of a mile along the upper border of a meadow 
area. 

ARTESIAN SPRINGS AT OASIS (MONO 20). 

Oasis is a small settlement lying northward from Deep Spring 
Valley, on the road from Owens Valley to Nevada. Springs of con- 
siderable size, whose yield is augmented by wells, furnish water 
for irrigating a number of acres. As at the springs in the valley a 
few miles southward, the artesian water of Oasis apparently rises from 
alluvium that deeply buries the bedrock and is probably suppHed 
from layers of gravel that act as storage reservoirs for the run-off 
from the surrounding mountains. 

BERTRAND RANCH SPRINGS (MONO 10). 

Tepid springs that rise on the Bertrand ranch in Spring Valley^ 
about 6 miles north of Benton, are used to irrigate a considerable 
area of meadowland. The water apparently rises under artesian 
pressure at the base of alluvial slopes, which are remarkably well 
developed along the flanks of the mountains that border the valley. 

RIVER SPRING (MONO 9). 

River Spring, about 10 miles in a direct line west of north from 
Benton, yields a considerable flow of water that is probably of 
alluvial artesian origin, and is otherwise similar in character to that 
of the springs a few miles to the southeast on the Bertrand ranch. 
It furnishes part of the supply of a small narrow lake around whose 
borders is a little meadowland. 



ARTESIAN SPRINGS. 323 

BLIND SPRING (MONO 13). 

Blind Spring, which is situated about 3 miles east of south from 
Benton, was formerly of some importance as a watering place, but 
of late years its flow, always slight, is reported to have nearly ceased. 
It is in open valley land and is said to have received its name because 
there was little growth near it to indicate the presence of water. 

ARTESIAN SPRING NEAR HOPLAND (MENDOCINO 30). 

A spring which is apparently of artesian origin issues on the Horst 
ranch, 1 mile north of Hopland. The water rises in a grove of willows 
at the mouth of a small ravine on the western edge of valley land 
along Russian River. The spring is protected by a board curbing, 
which forms a shallow pool 8 by 10 feet across, and the discharge — 
about 5 gallons a minute of faintly sulphureted water — is used to 
irrigate a vegetable garden. 

The adjacent hills are composed of the older sandstones and shales 
that form so large a portion of the Coast Ranges. Their structure, 
however, is not favorable to the occurrence of water under artesian 
pressure, and the spring is probably supplied by alluvial water that 
rises at this place. At the time of the earthquake of April 18, 1906, 
the spring ceased flowing for a short time but gradually returned to 
its normal discharge. 

ARTESIAN SPRINGS IN SHASTA VALLEY (SISKIYOU 13). 

A number of springs which rise in the northeastern part of the 
State are probably of alluvial artesian origin. Two of these that 
yield considerable water rise in Shasta Valley at points about 10 
and 1 1 miles southeast of Montague, one being known as Big Spring 
and the other as Little Spring. The former yields a large flow of 
water that is noticeably above the normal temperature; the latter, a 
mile farther south, yields a smaller flow of similar character. Both 
springs are used to irrigate tracts of meadowland but are capable of 
much more extensive development. 

ARTESIAN SPRING NEAR ALTXJRAS (MODOC 9). 

At the southern base of a low but extensive mound in meadow- 
land 1| miles southeast of Alturas is a spring of small flow at which 
a hydraulic ram has been installed that pumps the water to troughs 
in a corral on the mound. The observed discharge from the spring 
was only about 1 gallon a minute, but there was much seepage near 
it. The temperature of the water (72°) indicates that it is of deep- 
seated origin rather than of essentially siurface flow. It may rise 
from rock beds that underhe the vaUey alluvium and be similar in 
origin to the warm springs near Rattlesnake Creek (Modoc 8) and near 



324 SPEINGS OF CALIFOENIA. 

Canyon Creek (Modoc 7), to the northwest and to the southwest, 
which have been mentioned among the thermal springs. (See p. 120.) 

CABIN SPKINGS (LASSEN 18). 

Cabin Springs form a small roadside watering place on the border 
of Honey Lake Valley, about 4^ miles east of Amedee. There are 
five shallow depressions at the locaHty, 10 or 15 yards apart, and a 
quarter of a mile south of the lava slope that borders the valley. The 
western two are the largest, and when visited they contained small 
amounts of water of good quaUty, but there was no overflow. This 
water is thought to be essentially alluvial artesian in character. A 
number of years ago a small well three-quarters of a mile westward 
obtained flowing water, and three other wells which were sunk during 
the nineties about 3 miles westward also obtained small flows. 

In 1909 these four well's were still flowing, and each yielded from 1 
to 3 gallons a minute of water 71° to 78° in temperature. 

SELLICKS SPRINGS (LASSEN 9). 

Besides those springs in the lava-covered northeastern section of 
the State that have been mentioned as probably of alluvial artesian 
origin, there are a number of others which are thought to be in struc- 
tural artesian basins.^ Several large springs of constant flow rise on 
the borders of Secret Valley, in eastern Lassen County. Sellicks 
Springs, which form one of the largest groups, rise in a strip of meadow- 
land on the northern edge of the valley, about If miles northwest of 
Karlo railroad station. A careful float measurement of the stream 
flowing into the valley indicates that the discharge is about 1,050 
gallons a minute. The water is of good quahty and has a tempera- 
ture of 72°. The original belt of meadowland formed by it in the 
open vaUey south of the springs has been greatly increased by dis- 
tributing the water through ditches, so that nearly 300 acres of 
meadowland have been produced. A pipe also leads from the 
springs to a railroad watering tank at the station. 

TIPTONS SPRINGS (LASSEN 10). 

Tiptons Springs, at Secret post office, issue from the basaltic lava 
slope at the northern edge of the valley, 3 J miles east of Sellicks 
Springs. The water rises mainly in a marshy strip 150 or 200 yards 
long and flows at a rate measured at 925 gallons a minute (103 
miner's inches). The water flows southward and irrigates meadow- 
land, from which quantities of hay are cut. 

1 A structural artesian basin is formed where bedded rocks that mate a series of alternating relatively 
pervious and impervious layers are folded into a trough-shaped or saucer-shaped valley. Water collects in 
the lower portions of the more pervious beds under pressure of the water in the higher portions of the 
"ame beds around the borders of the valley. 



ARTESIAN SPRINGS. 325 

Springs similar to those nour the Tipton ranch house rise at three 
places between Sellicks anil Tiptons springs, along the edge of meadow- 
land on the south side of the road. One of these, which is about 1 
mile southwest of Tiptons, does not form a noticeable stream, but it 
makes a considerable meadow area. Two other springs rise at points 
about one-third of a mile and If miles west of it. Each of these 
western springs jdelds about 50 gallons a minute of water 60° to 64° 
in temperature. They form small areas of meadowland and also 
serve as watering places for cattle. 

SECRET SPRINGS (LASSEN 12). 

Secret Springs are on the southern border of the valley land, about 
4 miles east of Tiptons Springs. They yield a flow of perhaps 50 or 
60 gallons a minute that forms the usual meadow area, but their 
water has not been efficiently used. 

SHEEP SPRINGS (LASSEN 11). 

Sheep Springs, 4h miles northeast of Tiptons Springs, form a water- 
ing place for range cattle and have also been used to some extent for 
irrigating garden and meadow tracts. 

SPANISH SPRING (LASSEN 5). 

Spanish Spring issues on the slope 14 mUes north of the Tipton 
ranch, near the home of a settler in the region. The spring yields a 
considerable amount of water that has been used for domestic and 
garden supply. 

ARTESIAN SPRINGS ON SOUTH SIDE OF SHINNS PEAK (LASSEN 6). 

Springs that yield perhaps 100 gallons a minute of water noticeably 
above the normal temperature of this region (about 55°) issue on the 
southern side of Shinns Peak. Although they are at a considerable 
elevation above the valley land, it seems probable that, like others in 
the region, they issue from porous, tuffaceous beds and are of struc- 
tural artesian character. 

ARTESIAN SPRINGS NEAR SMOKE CREEK (LASSEN 7). 

Near the eastern border of the State water in considerable quantity 
issues from the slopes near Smoke Creek and forms a tributary of tliis 
stream. The rocks, as in most parts of Lassen County, consist of 
lava with interbedded tuffaceous layers that form excellent water 
carriers. 

ARTESIAN SPRINGS NEAR HEAD OF RUSH CREEK (LASSEN 13). 

Springs that strongly resemble those near Smoke Creek issue a few 
miles away on slopes near the head of Rush Creek and render it 
perennial in its upper course. They are too remote, however, to have 
become of use other than as a watering place for range stock. 



326 SPRINGS OF CALIFORNIA. 

ARTESIAN SPRINGS ON EAST SIDE OF HORSE LAKE VALLEY (LASSEN 8). 

In the western part of Lassen County there are a number of springs 
that are sunilar in character to those in the neighborhood of Secret 
Valley, which lies farther east. On the east side of Horse Lake 
Valley are springs that yield water of good quality and noticeably 
above the normal temperature of the region. These springs have been 
developed somewhat and are used by settlers on the valley land. 

ARTESIAN SPRINGS NEAR BAILEY CREEK (LASSEN 4). 

Near BaUey Creek, which is on the western side of Madeline Plains, 
there are springs of considerable flow that have been used mainly 
as watering places for cattle, but within recent years portions of the 
Madeline Plains (or Madeline Meadows) have been brought under 
irrigation and cultivation, and it is probable that all the minor avail- 
able flows of water will soon be utilized by settlers. 

ARTESIAN SPRINGS NEAR SOUTH END OF EAGLE LAKE (LASSEN 14). 

At the south end of Eagle Lake there is a considerable area of 
meadow that has been used for winter range and natural hay land for 
many years. A portion of it is irrigated by springs that are appar- 
ently of artesian origin, and other smaller springs of similar character 
issue on the lower slopes above the meadowland. 

Many other springs than those which have been individually 
referred to issue on the mountain slopes and along the valley bor- 
ders in Lassen County, but most of them have been used only as 
watering places on the stock range. As the region becomes more 
thickly populated, however, and the valley lands are brought under 
cultivation, the springs will become of much greater economic value 
and can be used to irrigate many acres. 

LARGE COLD SPRINGS. 

DISTRIBUTION. 

Cold springs of notable flow are found almost entirely in the north- 
eastern, lava-covered section of the State. They seem to be supplied 
by water of essentially surface origin, which sinks into the fissured 
lavas and porous tuffs and emerges at favorable localities. 

SPRINGS AT HEAD OF FALL RIVER (SHASTA 6). 

The largest of the cold springs — and probably the largest springs 
in the State — ^rise at the head of Fall River, one-fourth to three- 
fourths of a mile north of Dana post office, which is 56 miles by rail- 
road and stage east of Sisson. About six large springs rise on the 
borders of a meadow at the head of the river. Two of these rise 
about 250 yards apart on the southwest side of the meadow and 



LARGE COLD SPRINGS. 327 

flow eastward, uniting to form a stream that is perliaps 10 feet wide 
and 2 feet deep. The water of two other springs which rise 100 yards 
apart at the base of a gentle lava slope at the northwest edge of the 
meadow is distributed by ditches to ii-rigate the natural hay land. 
A large amount of water also issues at the northeast edge of the 
meadow about 500 3"ards cast of these springs, where a ])ond is 
formed by an earthen dam, so that the level of the water is raised to 
a height that renders it available for use on the meadow. Below 
this dam a stream 100 to 200 feet wide and 2 or 3 feet deep flows 
southward along the western base of a lava bank that borders the 
meadow. At several places along the margin of the stream and in 
its channel there are other springs of considerable flow. The most 
remarkable is about one-f^fth mile below the dam at the head of the 
stream. This spring rises in an oval pool about 50 by 60 feet across 
and 16 feet deep in a depression in the lava nearly 100 ^ards east of 
the main stream. Tlie water in this pool is very clear. It rises 
quietly but with a strong flow and joins the main stream 250 yards 
southward. The combined flow of the springs, or of Fall River, 
which they form, is 1,500 second-feet (675,000 gallons a minute).^ 
As the grade of the stream is low, water is not easily available for 
irrigation by gravity canals and has been used to relatively little 
extent. 

The springs rise at the southern border of an extensive lava field. 
They are locally considered to be the outlet of Tule or Rhett Lake 
at the northern border cf the State. The water may, however, be 
furnished by the precipitation on the lava fields to the north, for 
much the greater part of the water that falls on these fields sinks 
into the crevices and caverns in the rock, and there is very little 
direct surface run-off. A continual flow of 1,500 second-feet would 
be furnished by an annual run-ofi of 1 second foot from 1,700 square 
miles. This amount, 1 second-foot, is not excessive for the region 
under consideration, where the annual precipitation is 20 to 40 inches, 
for it represents both a normal run-off and the amount that usually 
sinks into the ground. There is an area of nearly 2,000 square miles 
of lava beds extending from northeast to northwest of Dana, and 
the topography of this area is favorable to the hypothesis that it 
may furnish the water of the springs at the head of Fall River. 

The temperature of the water, 53° to 54°, indicates that it is of 
essentially surface origin. 

LARGE COLD SPRING SOUTHEAST OF PITTVILLE (LASSEN 3). 

On JVIr. George Guthrie's ranch, 3 miles southeast of Pittville, or 
16 miles m a direct line southeast of the big springs at the head of 
Fall River, there is a spring whose water is probably essentially of 

1 Clapp, W. B., and Hoyt, J. C, Report of progress of stream measui-ements for the calendar year 1905: 
U. S. Geol. Survey Water-Supply Paper 177, p. 133, 1906. 



328 SPEINGS OF CALIFORNIA. 

surface origin, though its temperature (64°) indicates that it may 
rise from a depth of a few hundred feet. The spring was opened 
by Mr. Guthrie at the base of a slope of loose material and has been 
developed so that it yields about 900 gallons a minute of water of 
very good quality. It is used for domestic purposes and for irriga- 
tion on vaUey land that borders the course of Pit River. 

LARGE COLD SPRINGS ON BURNEY CREEK (SHASTA 9). 

During periods of normal and low water Burney Creek sinks at a point 
5 or 6 miles north of Burney Valley, but a short distance above Burney 
Falls, which are about 1^ miles above the junction of the creek with 
Pit River, the water issues again as large springs. The greater part 
of the water goes over the falls, but a large part also issues from fis- 
sures in the lava cliff, some distance below the crest of the falls. 
Although the water is apparently only that of the creek which sinks 
below Burney Valley and rises again farther down the course of the 
stream, it may be properly considered to issue as springs, whose chief 
difference from similar springs in the lava region is that the imme- 
diate source of the water seems to be evident. 

RISING RIVER (SHASTA 11). 

Rising River is a stream that flows from a small lake about 10 
miles east of Burney Valley, westward a distance of 2 or 3 miles to 
Hat Creek. The water rises in the lake and adjacent meadow, and its 
flow, which in July, 1910, was approximately 250 second-feet (112,500 
gallons a minute), is nearly uniform. The water has been used to 
some extent for irrigating meadow hay land, and by means of current 
wheels a small amount of water is lifted for dairy and domestic sup- 
phes. The source of the springs of Rising River is not so evident as 
is that of the springs on Burney Creek, but the water is locally (and 
plausibly) beUeved to be derived from Butte or Lost Creek, which 
flows from Lake Bidwell or Butte Lake to Porcupine Flat, where it 
sinks about 12 miles southeast of the head of Rising River. 

GREAT SPRINGS (SHASTA 12). 

Great Springs issue for a distance of about a quarter of a mile 
along the southwestern bank of Hat Creek, at the northern base of 
the mountain mass that culminates in Lassen Peak (PL XI). The 
greater part of the headwaters of Hat Creek is conducted westward 
by a power ditch, so that in July, 1910, there was a flow of only 
about 2 second-feet (900 gallons a minute) in its channel above Great 
Springs. Below the sprmgs the stream was 50 to 75 feet wide and 2 
or 3 feet deep, and a float measurement indicated a discharge of 280 
second-feet (126,000 gallons a minute). A portion of the water has 
been used for a number of years on the small ranches of Indians and 



LARGE COLD SPRINGS. 329 

white settlers along the lower coui-se of the stream, but only a small 
part of the supply has been employed. The water of Lost Creek ^ 
normally sinks at a (listance of about a mile above its j miction with 
Hat Creek, or about 2^ miles in a direct line west of south from Great 
Springs, and it is locally believed that the creek reappears in the 
springs. The position of the springs at the northern base of slopes 
that rise to Lassen Peak and the fact that the water issues almost 
entirely on that bank of Hat Creek which is toward the mountains 
indicate, however, that the supply comes mainly ft-om melting snow 
on the slopes to the south, though a part is perhaps derived from 
Lost Creek. The yield of the springs is said to vary somewhat with 
the season, a characteristic of springs that have near-by sources of 
supply. 

ROCK CREEK SPRINGS (SHASTA 13). 

Several cold springs of large flow issue on the western slopes of Las- 
sen Peak. Among them are Rock Creek Springs, which are near the 
headwaters of the stream of the same name. The water issues from 
a hard lava agglomerate at a rate of about 11 cubic feet per second 
(4,950 gallons a minute). Tliis water has been appropriated by the 
Northern Cahfornia Power Co. for use in generating electric power in 
their plant near Manton, several miles west of the springs. 

BIG CLIPPER SPRINGS (TEHAMA 1). 

Big CUpper Springs are similar in character and mode of occurrence 
to Rock Creek Springs. They issue about 4 miles in a direct line 
southeast of the latter, beside a tributary of Digger Creek, and yield 
a flow of about 5 second-feet (2,250 gallons a minute). Their water, 
like that of Rock Creek Springs to the northeast, has been appropriated 
for electric power generation by the Northern Cahfornia Power Co. 
The positions of both Big CHpper and Rock Creek springs and their 
large and nearly uniform flows indicate that, like other large cold 
springs in the region, their source of supply is the melting snow of 
Lassen Peak. The springs issue from layers of tuffaceous lava or 
lava agglomerate through which the water very probably percolates 
westward from the higher slopes until it finds surface escape in the 
creek canyons. 

LARGE COLD SPRINGS ON GERBER RANCH (TEHAMA 4). 

On the Gerber ranch, which is beside the stage road between Red 
Bluff and Paynes Creek post office and about 20 miles east of the 
former place, springs of considerable flow issue in a small meadow 
along the course of Paynes Creek. The water has supplied a small 
pond and has been used to some extent for irrigation. It is evi- 

1 This stream is 10 or 15 miles west of Butte Creek, which is also locally known as Lost Creek. 



330 SPRINGS OF CALIFORNIA. 

dently derived from the melting snow of the higher slopes to the east. 
The porous tuffaceous lava, which is known as the Tuscan tuff and 
which covers the slopes for some distance surrounding the springs, 
affords good storage for the water and renders the flow of the springs 
fairly uniform. 

LARGE COLD SPKINGS IN HOT SPRING VALLEY (PLUMAS 3). 

Large perennial springs of cold water issue from lava bluffs that 
form the north side of Hot Spring Valley, on the southeastern slope 
of Lassen Peak. The water issues about one-half mile west of 
Drake Hot Springs (Plumas 4, p. 142) at numerous places for a 
distance of 200 or 300 yards along the steep slope. The various 
streams flow down among small quaking aspens and unite to form a 
stream of fairly uniform flow that discharges approximately 1,500 
gallons a minute. A small part of the water has been used in irri- 
gating adjacent meadowland, but the main part of it flows directly 
into Warner Creek, of which it forms a tributary. 

In connection with these cold springs several minor ones in the 
same region may be mentioned. One that furnishes a domestic sup- 
ply at Drake Hot Springs issues 300 yards east of the house, from 
beneath a large lava bowlder on a steep slope below a bluff that borders 
the north side of Hot Spring Valley. This spring has a nearly uni- 
form flow of about 75 gallons a minute and is of interest because of 
its low temperature, which was 39° in July, 1910. Another un- 
usually cold spring but of less flow issues in meadowland at the 
head of Warner Valley, about 4 miles east of Drake Hot Springs. 
When visited this spring had a temperature of 44°, but its water was 
probably warmed somewhat by irrigation water from the creek. Its 
yield was only about 2 gallons a minute. Other cold springs that 
yield 5 to 20 or 30 gallons a minute issue in small meadow patches 
along tributaries of King and Warner creeks. On the barren slopes 
near the summit of Lassen Peak springs that discharge several second- 
feet issue along the sides of drainage channels during the season of 
melting snow. Their sources can often be recognized in melting 
snow banks a tew hundred yards away, and their mode of occur- 
rence helps to explain the existence of large springs on the lower 
slopes, where the source of supply is not so evident. 

LARGE COLD SPRINGS IN BIG MEADOWS (PLUMAS 8). 

Large springs issue at the northeast edge of Big Meadows, about 
5 miles by road northeast of Prattville. The water issues from ba- 
saltic lava, a few feet above the meadow level, in an area of willows 
and quaking aspens about 100 yards in diameter. After flowing down 
over riffles of coarse lava gravel it forms a sluggish stream 100 yards 
or more in width in the meadow. A very rough float measurement 



LARGE COLD SPRINGS. 331 

at the riffles indicates that the chscharge is about 56 second-feet 
(29,000 gallons a minute). The water is cold (46°) and of very good 
quality. It has been used to some extent for irrigating the meadow 
and forms a tributary of North Fork of Feather River. 

LARGE COLD SPRINGS ON BRANCH OF ROCK CREEK (PLUMAS 7). 

About 2 miles north of the springs in Big Meadows, springs of 
much smaller flow issue 50 yards south of the road between Pratt- 
ville and Susanville. The water rises in a marshy patch in a small 
swale on the lava slope and forms a stream that discharges perhaps 
1,000 gallons a minute. The water has not been used directly, but 
it flows southward to Rock Creek and thence into Big Meadows, 
where it irrigates a portion of the natural hay land. 

LARGE COLD SPRINGS EAST OF ROCK CREEK (LASSEN 15). 

About 3 miles northeast of the springs last described, or 2 miles 
east of Rock Creek, are other large springs that issue at the western 
side of a small escarpment in the basaltic lava and yield a stream 
whose flow was estimated to be perhaps 20 second-feet (9,000 gallons 
a minute) . Like the other springs of this region, their water has not 
been used directly, but it forms a tributary of Rock Creek. 

LARGE COLD SPRINGS NORTHEAST OF AGER (SISKIYOU 6). 

On the road to Klamath Hot Sin-ings, in a small ravine at the base 
of a butte of lava agglomerate about 9 miles northeast of Ager, cold 
water issues at several places from the talus slope at the western 
side of the butte and is collected in a ditch and used for irrigation. 
Water from one of the springs is also piped several hundred j^ards 
northward for domestic use at the home of the owner of the property. 
The temperature of the springs is 47°, and their combined flow is 
perhaps 1,400 gallons a minute. 

LARGE COLD SPRINGS NEAR LITTLE SHASTA RIVER (SISKIYOU 10). 

About 13 miles east of Montague, or 1 mile northeast of Table 
Rock Spring (Siskiyou 9, p. 219), there is a cold spring which yields a 
constant flow of about 6,300 gallons a minute (reported measurement, 
700 miner's inches). It rises from slopes of basaltic lava that form 
the mountains on the east side of Shasta Valley. The water is used 
in irrigating land near the spring, along Little vShasta River. 

LARGE COLD SPRING EAST OF MONTAGUE (SISKIYOU 12). 

A large spring that rises on Mrs. ]SI. F. ]Martin's ranch, near the 
southern base of Table Rock, 12 miles east of Montague, has been 
mentioned in connection with Martin Soda Spring (Siskiyou 11, p. 219) , 



332 SPRINGS OP CALIFORNIA, 

which rises near it. The cold spring issues in full volume from be- 
neath a small bank that is composed of lime-carbonate spring deposit 
and fragmental lava. It yields about 2,700 gallons a minute (re- 
ported measurement, 300 miner's inches) of water of very good 
quality that is used to irrigate meadowland to the west. 

LARGE COLD SPRINGS NORTH OF SISSON (SISKIYOU 17). 

A large amount of cold water rises in two springs at the west base 
of Black Butte, which is 1 mile north of Sisson, at the western base 
of Mount Shasta. The northern spring issues in a dense growth of 
vines and willows on the border of a strip of meadow and forms a 
stream carrying approximately 700 gallons a minute. The other 
spring, 125 yards southward, rises mainly in a cement-walled basin 
15 or 20 yards across. A part of its yield escapes to the meadow 
through an overflow weir, but the main flow is conducted in a canal 
southeastward and is used for irrigation. Measurements of the total 
yield of the two springs gave approximately 12,000 gallons a minute, 
of which about 85 per cent was flowing in the canal. These springs 
form the largest tributary at the head of Sacramento River and are 
sometimes referred to as its source. 

LARGE COLD SPRINGS AT HEAD OF MUD CREEK (SISKIYOU 16). 

At the head of Mud Creek, on the southern slope of Mount Shasta, 
are large cold springs whose water is muddy from suspended material 
that seems to be a glacial clay or rock flour. The source of the 
springs is evidently the snow of the higher slopes. 

LARGE COLD SPRINGS SOUTH OF McCLOUD (SISKIYOU 27). 

Cold springs rise in a small marshy area along a creek 1§ miles 
south of McCloud, in the basaltic lava plateau at the southern base 
of Mount Shasta. The water forms a stream of considerable flow, 
which has been mentioned in the description of Warmcastle Soda 
Springs (Siskiyou 28, p. 223). 

LARGE COLD SPRINGS ON EAST SLOPE OF MOUNT SHASTA (SISKIYOU 15). 

Cold springs that are similar to the others in the vicinity of Mount 
Shasta issue on its east ?lope. They form a stream that ip tributary 
to Ash Creek and through it to McCload River. Other cold springs 
of smaller size issue at a number of places on the slopes of Mount 
Shasta and form streams of nearly constant flow. The source of all 
the sprmgs is evidently the precipitation on the mountain. Con- 
siderable areas on its lower slopes are covered with coarse gravel 
that is probably of glacial origin. The town of Sisson is built on 



MINOR PERENNIAL SPRINGS. 333 

such material, and it is said to be difficult to obtain solid founda- 
tions for buildings at this place. It is said that men excavating in 
a railroad cut on the line from Sisson eastward to McCloud found 
ice interbedded with the gravel. The meltmg of large masses of ice 
that were covered by glacial gravel may partly supply several of the 
cold sprmgs, especially those at the head of Mud Creek, which seem 
to issue directly from glacial material. 

GLACIER SPRING (SISKIYOU 21). 

Several large springs issue along the course of Sacramento River 
near the base of Mount Shasta. Glacier Spring is a few feet below 
the brink of the river canyon and one-third of a mile by zigzag trail 
northeast of Shasta Springs station. It rises quietly in a circular 
cemented pool about 8 feet in diameter and 4 feet deep, in a concrete 
spring house. A 3-inch pipe leads down the slope to the railroad 
station, and the overflow — perhaps 50 gallons a minute — forms the 
head of a stream that cascades down the slope near the trail. The 
size of the stream is greatly increased by water which issues along 
its course, so that where it enters Sacramento River the stream has a 
winter flow of perhaps 6 or 8 second-feet. 

KEYSTONE SPRING (SISKIYOU 20 j. 

Keystone Spring rises on the plateau on the eastern side of the 
canj^on of Sacramento River, a short distance north of Glacier Spring. 
Its water has been piped to a tank and used for a domestic supply 
at Shasta Resort, which is situated south of the spring, near the 
canyon edge. 

Both Glacier Spring and Keystone Spring issue from crevices or 
fissures in the lava at the southern border of the plateau that ex- 
tends southward from Mount Shasta, and both are probably sup- 
plied by water derived from melting snow on the higher slopes. 

MINOR PERENNIAL SPRINGS. 

DISTRIBUTION. 

There are in the State many perennial springs of essentially surface 
origin that are well known to prospectors and other travelers and are 
of sufficient importance as watering places to have received names. 
Many of these are on well-traveled roads, but by far the greater 
number are in less knownti regions and are not easily accessible. 

In the northern part of the Sierra and in the Siskiyous and the 
northern Coast Ranges springs are numerous, but as there are also 
many streams in these well-watered regions the springs are of rela- 
tively little importance, though some of them supply roadside 
watering troughs. In the arid parts of the State, especially on the 
southwest side of San Joaquin Valley and in the eastern and south- 



334 SPEINGS OF CALIFORNIA. 

eastern sections, many springs of very small flow have become impor- 
tant because of their positions, for they may furnish the only water 
within a radius of 10 or 15 miles. Some of these desert springs yield 
water of poor quahty, as it contains noticeable amounts of alkaline 
salts, but as they afford in some places the only available supplies 
they are welcome watering places. 

The following descriptions cover most of the perennial springs 
which were visited or concerning which reliable information was 
obtained, together with a few minor fresh-water springs that are in 
the same localities as mineralized sprmgs which have been described. 

The springs are taken up in order from north to south along the 
eastern part of the State through the northern lava region, the Sierra, 
and the eastern and southeastern desert ranges, and then from south 
to north through the Coast Ranges. This order of discussion gives 
a convenient arrangement of the springs with regard to topographic 
and cHmatic conditions. 

Other springs of similar character but mainly of lesser importance 
are briefly described later under the heading "Springs that are less 
well known," but the locations of these springs are not shown on 
Plate I (in pocket) . 

POTHOLE SPRING (MODOC 1). 

A few springs of relatively small flow afford watering places for 
range cattle in the lava-covered region of western Modoc County. 
One of these, Pothole Spring, is situated in a small marshy area at 
the western base of Blue Mountain, about 35 miles northwest of 
Alturas. The water rises in a deep clear pool a few feet in diameter 
and is noticeably above the normal temperature but probably less 
than 70°. The flow is small and the water sinks in the marshland a 
short distance from its source. 

BOTTLE SPRING (MODOC 2), 

Bottle Spring is about 10 miles south of Pothole Spring and near 
the northern end of Fairchild Meadow. It yields cold water and the 
amount is said to vary greatly with the season. 

COOL SPRINGS AT CAMPBELL HOT SPRINGS (SIERRA 2). 

Two cool springs that furnish domestic supplies are situated on the 
grounds of Campbell Hot Springs, near Sierraville. These have been 
mentioned in the descriptions of the principal springs at the resort, 
and an analysis of water from the main cool spring has been given. 
(See p. 129.) Both cool springs are of slight flow, but they are con- 
veniently situated and 3deld good water for cooking and other 
household purposes. 



MINOR PERENNIAL SPRINGS. 335 

MUD SPRING (TEHAMA 6). 

A few small springs form watering places near the western base of 
the Sierra, on the slopes of tuffaceous lava that border Sacramento 
Valley in eastern Tehama County. Mud Spring rises in a rock-walled 
pool, 6 feet m diameter, at the northern edge of the county road, 13 
miles north of east from Red Bluff. Its water has been piped 200 
yards westward to a watering trough near sheepmen's corrals and 
camp, where the measured flow was about one-half gallon a minute. 

GEARY SPRING (TEHAMA 7). 

Geary Spring is similar to Mud Spring in character. It is about 
7 miles farther south at the side of a small drainage channel in the 
gentle, plateau-like slope. The water rises 50 yards south of a wagon 
road, in a rock-curbed pool, 3 feet in diameter, that is used as a water- 
ing and campmg place by travelers and stockmen. 

The water of Geary and Mud springs is of good quality, and their 
observed temperatures, which were respectively 66° and 62°, suggest 
that it rises from a depth of several hundred feet, probably from a 
layer in the bedded volcanic tuffs. 

HENDERSON SPRING (BUTTE 1). 

Henderson Spring issues from a steep bank of slate, in the bottom 
of the canyon of Big Butte Creek, 11 miles by road and trail, north 
of Stirling City. The water is said to have medicmal properties and 
has been used for a number of years by several residents of the region, 
but in the fall of 1909 no mineralization was noticeable to the taste. 
At this time, however, the water was diluted by storm water. The 
sprmg is not easy of access, as the canyon is steep and only a dim 
trail leads from prospectors' cabins on its upper slopes down to the 
creek and the spring. 

BLACK SPRING (MARIPOSA 1). 

In Yosemite Valley there are several perennial springs of cold 
water, of which Black Spring is perhaps the best known. It issues 
on the slopes on the northern side of the stage road, 4|- miles south- 
west of Yosemite post office, and is piped to the roadside, where it 
forms a watering place for horses as well as people. The water is 
cold and of excellent quality. 

MOSS SPRING (MARIPOSA 3). 

Moss Spring issues on the southern side of Yosemite Valley, about 
one-third of a mile south of Black Spring, in the lower land at the 
base of the valley wall. It is similar in character to Black Spring, 
but as it is not beside a main road its water has been little used. 



336 sPEiisrGS OP califoen-ia. 

FERN SPRING (MARIPOSA 2). 

About one-third of a mile west of Moss Spring another flow of 
cool, excellent water that is kno^vn as Fern Spring issues in the valley 
land, but like that of Moss Spring it has not been used. 

FOUNTAIN SPRING (TULARE 16). 

A few springs issue along the western base of the southern Sierra 
and have been used to some extent for domestic and garden supplies. 
Fountam Spring, which is about 15 miles east of south from Porters- 
ville, has long been known and utilized for such purposes. 

YANKEE SPRING (TULARE 17). 

Yankee Spring is situated about 20 miles south of Portersville, in 
the foothills that border the valley land. Like Fountain Spring it 
is well kno^vn in this region, and has long furnished a domestic and 
garden supply. 

WILLOW SPRING (KERN 5). 

A few perennial springs which are similar in character to the two 
last described issue on the slopes of the southern Sierra, some distance 
from the open land of San Joaquin Valley. Among them is Willow 
Spring, which is about 30 miles east of south from Portersville. Like 
the other springs of the region its water has been used locally to 
some extent. 

LANDERS SPRING (KERN 18). 

Landers Spring is in the basin of Caliente Creek, about 25 miles 
east of Caliente railroad station. It is a well-known watering place 
in this portion of the southern Sierra and is of local value as a water 
supply. 

BLACK LAKE SPRINGS (MONO 11), 

Black Lake is a narrow body of water, about 2 miles long, that lies 
on a plateau east of the Sierra, in Mono County. The southern end 
of its basin is about 2 miles west of and 900 feet above Benton, and 
during periods of high water the lake overflows down a steep rocky 
canyon past the settlement. The water has a dark color (possibly 
derived from decaying tules) which hag given the lake its name. The 
lake is said to be partly supplied by large springs that rise in it. In 
the fall of 1908 there was a tule swamp one-quarter of a mile long at 
the southern end of the lake, and beyond it a stretch of meadow 300 
yards wide and one-half mile long, extending to the head of the canyon. 
In the tule swamp about 25 pools were counted, ranging in diameter 
from 1 foot to 15 feet, with vertical banks and with depths apparently 
greater than their diameters. There was little overflow from the 
pools, but all contained cold water of good quality. At the southern 



MINOE PERENNIAL SPRINGS. 



337 



edge of the meadow a spring that yielded about 10 gallons a minute 
had been developed by a small cut in the granite slope. 

The water of Black Lake Sprmgs is apparently subsurface water 
from the suiTounding granitic slopes. It collects beneath the allu- 
vium that fills the narrow lake basm and rises to the surface in the 
numerous pools. 

The followmg early analysis shows that when the sample was col- 
lected the lake contained a concentrated primary alkaline water: 

Analysis of water from Black Lake, Mono County, Cal. 
[Analyst, Oscar Loew (1876). Authority, Wheeler report. Constituents are in parts per million.] 



Properties of reaction: 

Primary salinity 

Secondary silinity 

Tertiary salinity 

Primiry alkalinity 

Secondary alkalinity 

Tertiary alkalinity 

Constituents 

Sodium (Na) 

Potassium (K) 

Lithium (Li) 

Sulphate (SO4) 

Chloride (01) 

Bromide (Br) and iodide (1) 

Carbonite (CO3) 

Metaborate ( BOo) 

Phosphate ( PO4 ) 

Silica (SiOo) 



(?) 



By 
weight. 



Reacting 
values. 



7,224 


314.2 


375 


9.6 


Trace. 


Trace. 


2,449 


5L0 


1,422 


40.1 


Traces. 


Traces. 


6,980 


232.7 


Trace. 


Trace. 


Trace. 


Trace. 


50 


1.7 


18. 500 





BANNER SPRING (MONO 18). 

In the plateau region that extends southwestward from Benton 
there are a few small springs that are known to the Indian inhabitants 
and to prospectors. Banner Spring is one that is situated near a 
prospector's cabin 11 miles west of south from Benton. The water 
issues from gravelly material at the western base of a hill slope and 
in the fall of 1908 was piped to a watering trough near by, where it 
supplied about 3 gallons a ixdnute. 

MORAN SPRING (MONO 19). 

Moran Spring is 2 miles south of Banner Spring, at the place where 
the road branches eastward to the Casa Diablo mines and westward 
to Long Valley. The water seeps to the surface at the eastern end 
of a small meadow. Wlien it was visited there was no perceptible 
flow, but water of good quality stood in several shallow holes that had 
been dug. An Indian's cabin stood at the edge of a small cultivated 
field near by. Both Banner and Moran springs are in granitic material 
and the water seems to be essentially of surface origin. 
35657— wsp 338—15—22 



338 SPEINGS OF CALIFOENIA. 

SCOTTY SPRINGS (INYO 6). 

A number of springs of considerable flow issue along tlie eastern 
face of tlie Sierra bordering Owens Valley. One of the groups of 
largest flow is at Scotty Springs, on the mountain side about 12 miles 
in a direct line northwest of Independence and 1,800 feet above the 
valley. Three springs rise here at short distances apart in a small 
marshy area and yield a considerable flow which is tributary to 
Division Creek. 

SPRING NEAR STRING MEADOWS (FRESNO 3). 

Beside a trail between String Meadows and Rattlesnake Lake, in 
the northern extremity of Fresno County, there is a cold spring of 
rather unusual character, as it issues in full volume from beneath a 
small bank. It yields about 15 gallons a minute of water of excellent 
quality, and its position beside the trail makes it well known to 
travelers. 

THREE SPRINGS (FRESNO 7). 

Three Springs form a group rising a few yards apart in a small 
meadow on the higher slope of the Sierra. They yield a combined 
flow of perhaps 100 gallons a minute, but as there has not been a 
well-traveled trail past them they have not been well known nor often 
visited. 

RIVER SPRING (TULARE 6). 

A few cold springs of excellent water and large flow issue on the 
western slope of the high Sierra, south of those that have just 
been described. River Spring, which is one of the largest of these, 
issues on the slopes above Ninemile Creek, a tributary of North 
Fork of Kern River. The spring is about 4 miles by trail northeast 
of Jordan Hot Springs (Tulare 7, p. 53). The water rises in full 
volume from beneath a granitic bowlder, 3 or 4 feet in diameter, 
beside the trail and forms a stream of about 550 gallons a minute. 
Numerous small cold springs issue in the many meadows of the Sierra, 
but springs of such large flow as River Spring are not common. 

BARREL SPRINGS (INYO 9).i 

There are several perennial springs in the Inyo Mountains on the 
eastern side of Owens Valley. One group of these, well known 
locally, is Barrel Springs, in Mazourka Canyon, about 10 miles north- 
east of Independence, or 6 miles north of Citrus railroad station. 
The flow is small but of gdod quality and furnishes a supply for 
prospectors. 

1 The descriptions of a number of springs in southeastern California are taken from a report by W. C. 
Mendenhall (Some desert watering places in southeastern California and southwestern Nevada: U. S. Geol. 
Survey Water-Supply Paper 224). This paper contains also descriptions of many wells and of slightly used 
springs that are not shown on Plate I of the present paper. See also Bailey, G. E., The saline deposits of 
CaUfornia: California State Min. Bur. Bull. 24, May, 1902. 



MINOR PERENNIAL SPRINGS. 339 

SPRINGS NEAR SOUTHEAST SIDE OF OWENS LAKE (INYO 23). 

A sniaU amount of Avator of fail" quality issues iii a g^ouj^ of several 
springs along the southeast side of Owens Lake. The}^ are used by 
prospectors, who often camp near by, and they have long been a 
watering place on the road between Keeler and Mohave. The water 
is apparently of sm-face origin, coming from the slopes of the Coso 
Range to the south and rising in the alluvium of the lake basin. 

Similar springs issue a short distance toward the lake from the hotel 
at Keeler and yield a small amount of fair water. 

ARAB SPRING (INYO 24). 

In the Coso Range several springs of small but perennial flow fur- 
nish camping and watering places for prospectors and other travelers. 
Arab Spring is one of these on the road between Keeler and Coso 
mining camp. It is situated on the eastern side of the range about 
18 miles southward from Keeler. It is also known as Lower Cen- 
tennial Spring, Upper Centennial Spring being a similar spring in the 
same ravine a mile south and 400 feet higher. 

CRYSTAL SPRINGS (INYO 27). 

Crystal Springs, which are about 8 miles southeast of Arab Spring, 
also afford a watering place on the road to Coso, being 6 miles north 
of this camp. The yield is small but of very good quality. 

ROSE SPRING (INYO 25). 

Rose Spring forms a watering place that is well known to pros- 
pectors in the Coso Range. Tlie water issues near the western base 
of the range, about 4 miles south of Ilaiwee post office. 

The three watering places last described — Arab, Crystal, and Rose 
springs — are supplied by the precipitation on the adjacent mountains 
and are essentially surface springs, though they are of nearly constant 
yield. 

SPRINGS NEAR HAIWEE (INYO 26). 

Cold water issues from the coarse gravel slopes at the base of the 
Sierra, at a ranch that is 28 miles southward from Keeler and that 
was the Ilaiwee ; tage station in the fall of 1908. When the place was 
visited a flow of about 20 gallons a minute was collected by ditches 
along the side of a small cienaga or marshy area and was used for 
domestic supply and garden imgation. 

GRAPEVINE SPRINGS (KERN 13). 

Grapevine Springs are situated near the road between Keeler and 
Mohave and about 50 miles south of Ilaiwee. They yield a small 
flow of water of excellent quality. There is also running water during 



340 SPRINGS OF CALIFORNIA. 

most of the year in Grapevine Canyon, a mile or two above the 
springs. 

INDIAN WELLS SPRINGS (KERN 14). 

Springs that are similar in origin and character to those at Haiwee 
stage station issue from the gravel slopes bordering the Sierra at 
Indian Wells, a ranch that is about 53 miles southward from Haiwee 
on the road from Keeler to Mohave. The springs at Indian Wells 
yield perhaps 10 or 15 gallons a minute of water of good quaUty that 
is used for domestic supply and for irrigation. 

FREEMAN SPRINGS (KERN 15). 

Freeman post office is at a small ranch on the Mohave-Keeler road, 
about 6 miles southwest of Indian Wells. The place was formerly 
known as Coyote Holes, as water is obtained from shallow pits exca- 
vated where coyotes had dug a short distance to water. A continual 
flow of perhaps 3 or 4 gallons a minute has been developed on the 
gentle slopes of a wide drainage wash. 

SEARLES SPRING (KERN 16). 

Searles Spring is about 5 miles west of the post office of the same 
name, which is 15 miles by stage north of Randsburg. Water is 
piped from the spring to Searles station and furnishes a supply that is 
small but of good quality. 

SPRINGS AT SUMMIT DIGGINGS (SAN BERNARDINO 8). 

Summit Diggings form a small gold placer camp near the main road, 
6 miles north of Randsburg. The camp obtains an ample supply of 
water from several springs in the neighboring hills. 

RICARDO SPRINGS (KERN 19). 

Ricardo Spring's issue in the stream wash of a tributary to Red- 
rock Canyon, about 27 miles north of Mohave. They yield a small 
but perennial flow and have served as a watering place, the water 
being piped to a trough near the main road between Mohave and 
Keeler. During recent years the pipe line has not been kept in 
repair, but water has been obtainable at the springs. 

KOEHN SPRINGS (KERN 20). 

Koehn Springs, or Kane Springs, as the name is spelled on some 
maps, are on the western side of a dry lake of the same name about 
24 miles northeast of Mohave. The sprmgs yield only a small axnount 
of brackish water, but they have been of some importance as a road- 
side watering place. 



MINOK PERENNIAL SPRINGS. 341 

WATER STATION SPRINGS (KERN 21). 

Water Station, about 9 miles east of north from Mohave, has been 
a water-siij^ply point for many years on the Mohave-Keelor road. 
Shallow wells supply a portion of the water at this place, but water 
also rises to the surface m small springs near by. 

COTTONWOOD SPRING (INYO 16). 

A number of springs that are well Ituown to travelers are situated 
in the Panamint Range, which Hes between Owens Valley and Death 
Valley. One of the largest of these springs issues in the upper portion 
of Cottonwood Canyon, on the eastern side of the range, and forms a 
stream that usually flows for a couple of miles before sinking in the 
gravel of the wash. A main trail between Keeler and the north end 
of Death VaUey follows down the canyon. 

EMIGRANT SPRING (INYO 17). 

Emigrant Sj^ring is m Emigrant Canyon, which hes about 10 miles 
southeast of Cottonwood Canyon. The spring has been known since 
1852, when it was used by emigrants from Salt Lake City. Emigrant 
Canyon is still the main pass across the Panamint Range, so the 
sj)ring is a much-used watering place. The water issues in a wash 
at the base of a limestone chff 25 yards west of the road. The sup- 
ply is said to be about 1 gallon a minute, and the water is of good 
quahty. 

WILD ROSE SPRING (INYO 22). 

Wnd Rose Spring is in a canyon on the western side of the Pana- 
mint Range, about 14 miles south of Emigrant Spring and 20 miles 
north of Ballarat mining camp. It forms a much-used camping place 
on the road to Death Valley by way of Emigrant Springs. The water 
is very good and the supply is plentiful. 

Like most of the springs in the desert ranges, Cottonwood, Emi- 
grant, and Wild Rose springs are supphed only by the precipitation 
on the adjacent higher slopes, but their subsurface storage reservoirs 
are sufficiently large to niake them of perennial flow, and hence 
they are dej^endable watering places. 

LONE WILLOW SPRING (SAN BERNARDINO 1). 

There is a spring in a small canyon near the pass between the Slate 
Range and Brown Mountain at the south end of Panamint Valley 
that is well known to travelers in the region, for not only is its water 
very good, but it is the only water to be had for a number of miles. 
The spring received its name. Lone Willow, from a tree that once 
grew near it. The water was formerly piped to troughs at the road- 
side, where it furnished one of the watering places on the route of the 



342 SPRINGS OF CALIFORNIA. 

'' 20-mule teams " that hauled borax from Death Valley to the railroad 
at Mohave. 

TULE SPRINGS (INYO 28). 

Water of poor quahty issues at a few places in Death Valley and is 
obtained from shallow wells at a number of other places in the valley 
floor. One of the groups where water naturally rises is at Tula 
Springs, beside a wagon road on the western side of the lowest por- 
tion of the valley. There are several springs, which are marked by 
clumps of tules, but the water is brackish and of small quantity. 

BENNETTS WELLS (INYO 33). 

Five miles south of Tule Springs there are other springs of better 
quahty, which have been protected by barrels and are known as 
Bennetts Wells. These springs or wells are marked by clumps of 
tules and by abandoned works of the Eagle Borax Co. They were 
formerly much used as a watering place, but they have not been of so 
great importance during recent years and they are occacionally 
choked by drifting sand. The water of Tule Springs and of Bennetts 
Wells is evidently of alluvial origin and is probably derived from the 
precipitation on the eastern side of the Panamint Range. It possibly 
rises under slight artesian head, but the supply is so small that the 
water becomes saline and alkaline from the salts near the surface. 

SAND SPRING (INYO 10). 

Sand Spring is in Termination Valley, at the extreme north end of 
the Grapevine Mountains, beside a road that extends northward along 
the base of these mountains and eastward into Nevada. The spring 
yields a small amount of good water and has long been used as a 
camping place. 

STAININGEB, RANCH SPRINGS (INYO 11). 

In the Amargosa Range of mountains, on the east side of Death 
Valley, there are several springs that form watering places which are 
well known to desert travelers. One of the northern of these watering 
places is at the Staininger ranch, in a canyon on the western slope of 
the north end of Grapevine Mountains. This ranch is on the road 
that leads southwestward into Death VaUey from Bonnie Claire 
railroad station in Nevada. The ranch is supplied with water by 
several springs of ample yield. 

DAYLIGHT SPRING (INYO 13). 

A main road from Bullfrog, Nev., southwestward into Death 
Valley, crosses the Amargosa Range through Boundary Canyon, 
which is between the Grapevine and the Funeral mountains and 30 
miles in a direct line southeast of the Staininger ranch. Daylight 



MINOR PERENNIAL SPRINGS. 343 

Spring, which furnishes a watcrmg phicc on tliis road, near tlie i)ass, 
issues a short distance north of the summit, on the hillside 300 yards 
west of the road, and yields a seeping flow of good water. 

KEANE SPRING (INYO 14). 

Keane Spring has a somewhat larger flow than Daylight Spring 
(Inyo 13). It issues on the western slope of the mountains, about 3 
miles southwest of Daylight Spring, in a large wash some distance 
south of the main road. 

Like most of the desert springs, those in the Amargosa Range are 
of essentially surface origin, and the two last described are hardly more 
than seepages, but they are of sufficient permanence to be dependable 
watering places and have long been used by travelers. 

CHINA RANCH SPRINGS (INYO 36). 

The China ranch is situated in the canyon of WiUow Creek, liaK a 
mile or more above its junction with Amargosa River and 5 miles 
north, of Sperry station on the Tonopah & Tidewater Railroad. 
Willow Creek is supplied by springs of considerable flow and of good 
quality, which issue from sandstones and clays of Tertiary age that 
form the canyon walls. The water is used to irrigate several acres of 
alfalfa and garden vegetables, and the ranch forms one of the few 
oases in the desert eastern part of the State. It is a stopping place 
and supply point on one of the main desert routes between the mining 
camps of eastern California and western Nevada. The springs were 
visited by Fremont in 1844, when returning eastward from his 
exploring expedition. 

OWL SPRINGS (SAN BERNARDINO 5). 

A number of small springs in the detached desert mountains and 
ranges of San Bernardino County form watermg places on the prin- 
cipal routes of travel, these routes being, indeed, largely determined 
by the locations of the springs. Owl Springs are on the road that 
leads southwestward from South Death Valley to Randsburg, and 
are about 2 miles north of the pass between Owl Mountains and 
Avawatz Mountains. The water issues as seepages in trenches and 
pits that have been dug in a wash. It is slightly saline but is the 
only supply on the road for about 17 miles in either direction. 

LEACH S SPRINGS (SAN BERNARDINO 7). 

Leachs Springs, about 17 miles by road southwest of Owl Springs, 
form one of the principal camping places between South Death Valley 
and Randsburg. They are in a canyon on the northern side of Leach 
Mountain, 3 or 4 miles south of the direct course of the road, but most 
travelers leave the main road and make a night camp at the springs. 



344 SPEINGS OF CALIFORNIA. 

There is one main spring that supplies a small pool 100 yards from the 
camp ground, and other seepages issue for perhaps 200 yards up the 
canyon. The water is obtained in the gravel of the canyon bed and 
is of good quality. 

CAVE SPRINGS (SAN BERNARDINO 6). 

Cave Springs are near the summit of Avawatz Mountains, on a road 
that leads from South Death Valley to Daggett. The water issues in 
grottos or caves in two pools about 5 feet across that form collecting 
basins from which it may be dipped. It is of good quality and the 
place is one of the principal stopping points on the road. The nearest 
other water to the north is at Saratoga Springs (San Bernardino 3), 
which have been described among the hot springs (p. 137). 

TOMASO SPRINGS (SAN BERNARDINO 12). 

Tomaso Springs are at the northwest end of Soda Lake Mountains, 
about 12 miles southwest of the town of Silver Lake, which is on 
the Tonopah & Tidewater Railroad. The springs are mentioned 
by Fremont, who camped at them in April, 1844, and later they 
became a watering place on the emigrant road from Salt Lake City. 
They are still used by campers, but they have become of less im- 
portance since the construction of the railroad and the establishment 
of a pumping plant at Silver Lake. 

DANTE SPRINGS (SAN BERNARDINO 13). 

Dante Springs are near the north base of a butte at the northeast 
end of Soda Lake, and are about 3 miles east of Berry station, on the 
Tonopah & Tidewater Railroad. They furnish a watering place 
on the main route from Soda Lake Mountains, which are west of 
Berry, to Ivanpah Mountain, 35 miles to the northeast. 

HALLORAN SPRINGS (SAN BERNARDINO 14). 

Halloran Springs are near the base of a small butte aboat 12 miles 
east of Dante Springs. They have long been a camping place on the 
mam route through this region and furnish a small bat ample supply 
for desert travelers. 

KESSLER SPRINGS (SAN BERNARDINO 15). 

Kessler Springs are situated at the southern end of Ivanpah 
Mountain, near the eastern border of the State, about 6 miles north- 
west of Cima station, on the Salt Lake Railroad, and at the junction 
of roads to the mining camps of Rosalie and Ivanpah, which are, 
respectively, 12 miles northwest and 10 miles northeast of the 
springs. The water is of very good quality, and the supply is plenti- 
ful. 



MINOR PERENNIAL SPRINGS. 345 

ROCK SPRINGS (SAN BERNARDINO 16). 

Rock Springs are about halfway between the Salt Lake and the 
Santa Fc railroad lines, near the eastern border of San Bernardino 
County, on the old Government road to Fort Mohave, Nev. They 
yield a small amount of water of good quality — the only water for a 
number of miles. 

PIUTE SPRING (SAN BERNARDINO 17). 

Piute Spring is situated in Piute Pass, on the old military road to 
Fort Mohave, Nev., about 9 miles east of Blackburn railroad siding. 
It forms a watering place that is well knowai to prospectors, and 
yields a small amount of water of good qualit}". 

VONTRIGGER SPRING (SAN BERNARDINO 18). 

Vontrigger Sprmg is about 6 miles southwest of Piute Spring, 
on a road that leads to Goffs station, on the Santa Fe Railway, 9 
miles southward. The water issues in a small canyon on the southern 
side of low hills, 2 miles north of Vontrigger, and like that of Piute 
Spring is of good quality and sufficient in quantity for travelers. 

KLINEFELTER SPRINGS (SAN BERNARDINO 19). 

Klinefelter is a station on the Santa Fe Railway, near the eastern 
border of the State. The railway company has installed tanks 
here for locomotive supply, the water being obtained from large 
springs that rise in the gravel of Sacramento Wash. In addition 
to the main springs, considerable water seeps from the banks at several 
places along the railway. The locality is the mam source of water 
supply for prospectors m the mountains to the south. 

SPRING NORTHEAST OF VICTORVILLE (SAN BERNARDINO 21). 

At the southwest side of a northern spur of Granite Mountain, 14 
miles northeast of Victorville, on the road between that place and 
Daggett, is a spring that yields a small flow of good water and was 
formerl}'' the main watering place on this road. Within recent years, 
however, other supplies of water have been made available by wells 
that have been sunk several miles to the southwest. 

ORD SPRING (SAN BERNARDINO 22). 

Ord Spring is at the western base of Ord Mountain, about 18 
miles south of Daggett, on a road that leads to San Bernardino 
Mountains. It yields water of good quality and is an old camping 
place that is well known to prospectors. 



346 SPRINGS OF CALIFORNIA. 

LE CONTE SPRING (SAN BERNAKDINO 23). 

Le Conte Spring is on the eastern side of Ord Mountain, about 10 
miles in a direct line eastward from Ord Spring. It forms a camping 
and watering place on a road between Newberry railroad station and 
Victorville. 

PEACOCK SPRING (SAN BERNARDINO 24). 

Peacock Spring forms a watering place at the northern base of a 
western extension of the Bullion Mountains, 10 miles south of Lavic 
railroad station. It is on a road that leads southward to San Ber- 
nardino Mountains and is important because it furnishes the only 
water between Lavic and a well near a dry lake 15 or 20 miles to the 
southwest. 

SURPRISE SPRING (SAN BERNARDINO 40). 

Surprise Spring is in the open desert southwest of Bullion Mountains, 
on a road that leads to mining camps farther southeast. It 5delds 
water that is somewhat alkaline, but it is used by travelers. The 
spring receives its name because it is located in open land where 
natural springs are not to be expected. 

MESQtriTE SPRING (SAN BERNARDINO 42). 

Mesquite Spring is about 12 miles southeast of and in the same 
desert flat as Surprise Spring. It forms a camping place where the 
water is of better quality and more abundant than at the northern 
spring. 

Both Mesquite and Surprise springs are in a shallow desert trough 
and are probably points at which water rises to the surface through 
the desert alluvium under a slight artesian head. Other springs 
similar in character rise in the southern portion of the flat, at 
Twenty-nine Palms Springs (San Bernardino 44, p. 316). 

BOX S SPRING (SAN BERNARDINO 28). 

Several perennial springs issue in San Bernardino Mountains and 
supply small ranches, prospectors' camps, or cattle- watering troughs. 
Box S Spring is one of these desert springs that is situated at the 
northern base of the mountains, about 10 miles west of Old Woman 
Springs (San Bernardino 27, p. 316), at the foot of the road grade 
up the mountain. Its water seeps from a bank of decomposed granite 
at a rate of about 1 gallon a minute and is piped to a county watering 
trough at the roadside. 

CUSHENBURY SPRING (SAN BERNARDINO 29). 

Cushenbury Spring rises in a small area of marshy land near the 
base of the steeper slope of San Bernardino Mountains and is on the 
road about 2J miles southeast of Box S Springs. It forms a small 



MINOR PERENNIAL SPRINGS. 347 

tiile-grown stream that has a flow of about S gallons a minute 
near the road. It sujiplies a watering trough and has also been used 
for garden irrigation. 

CACTUS FLAT SPRING (SAN BERNARDINO 30). 

Cactus Flat Spring, which is also knowii as Hidden Spring, issues 
from an adit excavated m the hartl, granitic material in the side of a 
ravine. The water is collected in a small reservoir formed by a dam 
across the ravine, and has been used for more than 20 years for 
domestic supply and for irrigation. It furnishes a convenient water- 
ing place on the stage road from Victor^dlle to Bear Valley. 

SARAGOSSA SPRING (SAN BERNARDINO 31). 

Saragossa Spring is about 2 miles in a direct line or 3 miles by road 
southwest of Cactus Flat Spring. It has been developed by an 
excavation in gTay granitic material and yields a small domestic 
supply that is of value m this poorly watered portion of the moun- 
tains. 

MONTE CRISTO SPRING (SAN BERNARDINO 32). 

Monte Cristo Spring is in Van Dusen Canyon, a mile or more in a 
direct hne southward over Gold Mountain from Saragossa Spring. 
It ^nelds about 1 gallon a minute of cool, fresh water that supphes 
the camp of the Rex Mining Co., which has been driving the Monte 
Cristo tunnel into the mountain. 

WARRENS RANCH SPRINGS (SAN BERNARDINO 39). 

Warrens Ranch Springs are situated a number of miles southeast 
of Cactus Flat, in a pass on the opposite slope of the mountains. 
The ranch is 28 miles eastward from Baiming, on the mam road to 
Dale mining camp, and is a regular stoppmg place for travelers. Its 
water is obtained from large springs below the ranch and is pumped 
to it by a gasoline engine. 

The springs at the six localities last described (San Bernardino 28, 
29, 30, 31, 32, and 39) are among those principally used of the 
numerous springs that rise m San Bernardino Mountains. All of 
them are of surface origin and owe their permanence to the precipi- 
tation on the slopes of the mountain range, whose higher peaks are 
capped with snow during a part of the year. 

PALMDALE SPRINGS (RIVERSIDE 12). 

An agricultural settlement was started at Palmdale, 8 miles south 
of Palm Springs railroad station, a number of years ago, but in 1909 
the place was nearly abandoned. Water for irrigation was furnished 
partly by a group of springs that yield a considerable supply. 



348 SPEINGS OF CALIFOENIA. 

COTTONWOOD SPRINGS (RIVERSIDE 20). 

Cottonwood Springs, on the road from Mecca to Dale mining camp, 
form a camping place that is well known to prospectors. They are 
in a pass in the Eagle Mountains, 26 miles by road northeastward 
from Mecca. The water seeps from granite and collects in a small 
concrete reservoir from which a pipe line extends northward to the 
Iron Chief mine. The water is of very good quahty, as is that of 
most of the desert sprmgs that issue from granitic rocks. 

CORN SPRINGS (RIVERSIDE 22). 

A stream of perhaps 50 gallons a minute rises in a small cienaga at 
Corn Springs, on the eastern side of Chuckwalla K^ . nii. The 
springs form a camping place on one of the desert lines of travel to 
mining prospects in the mountains farther east. 

FRINK SPRINGS (IMPERIAL 2). 

Frink Springs are on the eastern side of Salton Sink about 6 miles 
northwest of Frink station on the Southern Pacific Raihoad. A 
wagon road between San Bernardino and Yuma, which was much 
traveled before the construction of the railroad, passes the springs, 
and they were formerly an important watering place. They are still 
of considerable importance, as they furnish the only water for a dis- 
tance of several miles along the eastern side of the Sink. The water, 
which is of good quality, rises in small amount from sedimentary 
material. 

MILL CAMP SPRINGS (RIVERSIDE 21). 

Mill Camp is a mining camp on the western side of Chuckwalla 
Mountains and is 30 miles by road eastward from Salton. Good 
water in abundance is furnished by springs at the settlement. 

MULE SPRINGS (RIVERSIDE 23). 

Mule Springs are in the main pass on the west side of Palo Verde 
Mountains, near the southeast border of Riverside County, on a road 
between Mecca and the settlement of Palo Verde. The springs yield 
considerable good water, and their position is marked by a grove of 
small trees. 

SUNSET SPRING (IMPERIAL 7). 

Considerable water rises in a tule area at Sunset Spring, which is 
about 13 miles south of east from Brawley, in the Imperial Valley. 
The spring has been known for many years, but it has been used 
mainly by desert animals. Since the settlement of Imperial VaUey 
and the introduction of irrigation the spring has become of even less 
importance as a watering place for travelers. 



MI.VOH T'EHKNNIAL SI'HIX<;S. 349 

BOEEGO SPEING fSAN DEEGO 6). 

A few perennial springs of small flow issue in the hilLs on the 
western side of Colorado Desert and form watering places on the 
main lines of travel. Borego Spring, one of these watering places, is 
on the west bank of a broad wash, 33 miles by road northeastward 
from the mining town of Julian. The water rises in a small area of 
salt grass and rushes. It is alkaline but is the only water to be 
obtained in the locality. 

VALLECITO SPRINGS rSAN DEEGO 8). 

Vallecito Springs are about 33 miles Vjy road south of east from 
Julian. The locality, which was formerly a station on one of the 
stage lines between San Diego and the East, is still marked by an 
adobe building, and a trough near it affords a convenient watering 
place. Water of fair quaUty issues at these springs, which are in a 
small valley along Vallecito Creek. 

CARRIZO SPRINGS (^SAN DEEGO 11). 

Carrizo Springs lie about 18 miles eastward from Vallecito Springs. 
This place also was formerly a station on the overland stage road, 
which is still the main route between Julian and Imperial Valley, 
and the springs form a much appreciated watering place. The water 
issues in the wash of Carrizo Creek in a number of springs that furnish 
suppUes of fair quahty. A considerable flow of more alkaline water 
rises in a tule marsh near by. 

Clay beds of Tertiary age that are eroded into a typical bad-land 
surface lie against the mountain slopes at this locality. 

MASON RANCH SPRINGS rSAN DIEGO 10). 

The Mason ranch is about 5 miles northeast of Carrizo Springs. 
It is supplied by springs of good quality that have been in part 
developed in the slopes of the locality. The ranch forms a watering 
place that is well kno^vn to travelers over the road past it. 

MOUNTAIN SPRING (^SAN DEEGO 18). 

Mountain Spring is close to the southern border of the State, on one 
of the main roads between San Diego and Imperial Valley. It has been 
used as a watering place since the days of the stage line from San 
Diego to Yuma, when there was a station at the spring. The water 
issues in a ravine near the top of a steep grade down to the valley land 
and is piped to a trough at the roadside. It is of very good quahty 
and of ample flow. In recent years it has been improved by the 
county for the use of travelers. 



350 



SPRINGS OF CALIFORNIA. 



LA MESA SPRING (SAN BIEGO 14). 

La Mesa Spring is beside a small drainage swale haK a mile south- 
east of La Mesa raUroad station, or 11 miles by railroad northeast of 
San Diego. It was formerly known as Indian Spring, as it was a 
favorite camping place for a few families of Mission Indians. A few 
years ago the spring was inclosed by a small building, and a bottling 
house was erected, but when the spring was visited in the summer of 
1908 the water had not been placed on the market. A faucet near 
the house enabled campers and local residents to obtain the water. 
It is slightly alkaline and has a faint odor of hydrogen sulphide. At 
the spring the granitic rock is much decomposed, and the bed of the 
swale is covered with dark-colored alluvial soil. 

EL GRANITO SPRING (SAN BIEGO 13). 

El Granito Spring is at the base of the granitic slopes at the southern 
border of El Cajon Valley, 16 mUes by raOroad northeast of San Diego. 
The water issues in a small tunnel in decomposed granite at the side 
of a ravine and is piped about 50 yards to a bottling house. It has 
been on the local market for several years as a table water. The fol- 
lowing analysis indicates that the water is primary sahne and sec- 
ondary alkahne in character and also has notable primary alkahnity. 



Analysis of water from El Granito Spring, San Diego County, Cal. 
[Analyst, Joseph Luce. Authority, advertising matter. Constituents are ia parts per million.] 



Temperature 

Properties of reaction: 

Primary salinity 

Secondary salinity . . . 

Tertiary salinity 

Primary alkalinity. . . 
Secondary alkalinity. 
Tertiary alkalinity. . . 



Constituents. 



17° C. (62° F.) 

55 


14 
31 
14 



By 

weight. 



Reacting 
values. 



Sodium (Na) 

Potassium (K)... 

Calcium (Ca) 

Magnesium (Mg). 
Iron ( 



^(Fe). 



Aluminum (Al). 
Sulphate (SO 4).. 
Chloride (01).... 
Carbonate (CO3). 
Silica (SiOs) 



Carbon dioxide (CO2)- 



138 
a 190 
•4.8 
58 
Trace. 
5.4 
383 
26 
208 
16 



5.98 
4.87 

.24 

4.80 

Trace. 

.54 
7.98 

.72 
6.95 

.53 



1,029.2 



38 



1.73 



a Probably too high, since as reported it is considerably in excess of the sodium. 
BRADLEY SPRING (SAN DIEGO 7). 

Bradley Spring is 6 miles by road northward from the railroad ter- 
minus at Foster station, or 30 miles northeast of San Diego. The 
water issues at the base of a granitic bowlder in a steep brushy 



MINOR PEKENNIAL SPEINGS. 



351 



ravine, 250 feet above the road. A cciueiitod reservoir in the ravine 
collects the water, which has been piped to a storage tank at the road- 
side, whence it has been taken to San Diego and bottled as a table 
water. The spring seems to be of seepage flow and of essentially 
surface origin. 

COKONA SPRING (SAN DIEGO 5). 

A number of cold sprmgs of excellent water rise along the southern 
border of "Warner Valley, which is m the mountains about 60 miles 
by road northeast of San Diego. One of these springs was developed 
commercially a few years ago, and its water was placed on the local 
market as a lithia table water. The following analysis shows that 
it is a slightly mmeralized water, primary alkaline and salme and 
secondary alkaline m character. The rather large proportion of 
lithium rep(n'tcd is noteworthy. 

Anahjds of water from, Corona Spring, San Diego County, Cal. 
[Analyst, Joseph Luce. Authority, advertising matter. Constituents are in parts per million.] 



Properties of reaction: 

Primary salinity 

Secondary salinity 

Tertiary salin.ty 

Primary alkalinity 

Secondary alkalinity 

Tertiary alkalinity 

Constituents 

Sodium (Na) 

Potassium (K) 

Lithium (Li) 

Calcium (Ca) 

Magnesium (Mg) 

Iron ( Fe) 

Aluminum ( Al) 

Sulphate (SO4) 

Chloride (Cl) 

Carbonate (CO3) 

Silica (SiOs) 




In 190S the water rose in a small cemented basin at the base of a 
15-foQt bank of black alluvium in the first ravine east of the road 
grade from Mesa Grande northward down into Warner Valley. A 
scum of brown iron-colored deposit, probably the vegetable growth 
known as Crenothrix, covered the surface of the water, and a few large 
bubbles rose in the basin. A pipe extended thence 200 yards down 
the ravme to the valley edge, where the water had been run into 
tanks and taken to San Diego for bottlmg. The water at the lower 
end of the pipe had a distinctly sulphureted odor. The discharge of 
the sprmg was approxmiately 30 gallons a mmute. 



352 SPEINGS OF CALIFOENIA. 

A similar spring of smaller flow issues a few yards below the road 
grade, half a mile northwest of Corona Spring, and forms a roadside 
drinking spring. Two others of larger flow, that have not been used, 
issue in a ravine about 3 miles southeastward. 

DAVIS SPRING (SAN DIEGO 3). 

There is a spring of excellent water 2 miles northward from Nellie 
post office in the Palomares Mountains, 30 miles by road northeast of 
Escondido. The water issues at the base of a large alder tree 20 
yards from a creek bed and is much used and appreciated by campers 
during the summer time. A small amount of iron is deposited at 
this spring, and larger amounts are m evidence at a lesser spring at 
the creek edge. Numerous other springs of cold water issue in marshy 
areas in this part of the mountains. 

CONSOLE SPRING (RIVERSIDE 1). 

On the granitic slopes a few miles east of Riverside there are a few 
small springs that have been utilized. One of these, which is known 
as Console Spring, issues in Reche Canyon, about 9 miles in a direct 
line east of Riverside, and yields perhaps 7 gallons a minute. The 
water was placed on the local market m 1906 as a table water. A 
partial analysis, pubhshed in advertising matter, indicates that the 
water contains about 250 parts per million of solids in solution, 
sodium, carbonate, and sulphate being the principal constituents. 

BOX SPRING (RIVERSIDE 2). 

Box Spring is beside the railroad in a small ravine 5 miles in a direct 
line southeast of Riverside and near the head of the grade to Alessan- 
dro and Ferris valleys. A section house stands near the spring, 
which has been curbed and forms a domestic supply for the section 
hands. The spring yields a small flow of water of good quality. A 
similar but unused spring is situated in Mockingbird Canyon, 9 miles 
south of Riverside. 

ROSE SPRING (LOS ANGELES 12). 

A number of local natural waters are marketed in the larger cities 
of the State for table use, as they are preferable to the municipal 
supplies. Several waters are distributed in Los Angeles, but most of 
them come from wells. A few of them are derived from springs, 
however, of which Rose Spring is one of the chief. In the early 
days of the city it formed a roadside watering place on the eastern 
outskirts, but it is now well within the city limits. The water issues 
from crevices in a sandstone bank beside one of the principal avenues. 
It is piped a few yards to faucets in a bottling house, where 1-gallon 



MINOK PERENNIAL SPRINGS. 



858 



and 5-gallon bottles are filled for the trade, and it lias been on the local 
market since about 1900. The followmg analysis shows that it is a 
primary saline and secondary alkaline water: 

Anabjsis of water from Rose Spring, Los Angeles County, Cal. 
[Analyst, not given. Authority, advertising matter. Constituents are in parts per million.] 



Properties of reaction: 

Priraary salinity 

Secondary salinity 

Tertiary salinity , 

Primary alkalinity 

Secondary alkalinity 

Tertiary "alkalinity 

Constituents, 

Sodium (Na) 

Potassium (K) 

Calcium (Ca) 

Magnesium (Mg) 

Iron(Fe) 

Aluminum (Al) 

Sulphate (804) 

Chloride (CI) 

Carbonate (CO3) 

SiU ca (SiOs) 




KENTUCKY SPRINGS (LOS ANGELES 2). 

Small springs of perennial flow issue at a few places in the more arid 
parts of the southern Coast Ranges and are important watering places 
for cattle. Some of these springs also furnish good sites for apiaries, 
as the bees may there easily obtain water. Kentucky Springs have 
been used for both of these purposes. Tliey are situated about 4 miles 
south of Vincent railroad station, in the hills that border the south- 
western side of Mohave Desert. Three seeping flows here issue in a 
small ravine, and the water from the principal one has been piped to 
a watermg trough. A flow of approxunately 10 gallons a mmute was 
observable in July, 1909, and this yield could be considerably increased 
by cleaning the springs out to solid rock. The region is granitic, and 
the slopes are covered with a mantle of rock debris in which the supply 
of the springs is stored by the winter rains. 

There are other springs similar in character to Kentucky Springs 
at points 3 miles south, 3 miles southeast, and 2 or 3 miles northward. 

GRAVES SPRING (KERN 23). 

Near the border of the valley land westward from Rosamond rail- 
road station on the western side of Mohave Desert are small springs 
whose waters have been utilized. The western one, which is known 
as Graves Sprmg from the name of the owner, is 3 miles from Rosa- 
mond. A basin 3 or 4 feet square has been excavated at the spring, 
35657°— wsp 338—15 23 



354 SPEINGS OP CALIFORISriA. 

and the water is piped a few yards to a board-curbed pool that forms 
a watering place for cattle. In July, 1909, the visible flow was about 
1 gallon a minute of water of good quality. 

SPRINGS NORTHWEST OF ROSAMOND (KERN 24). 

Springs that are similar to the one just described issue a mile north- 
eastward and higher up on the slope. They have been used as a 
water-supply point and a camping place by prospectors. The water 
issues at two points a few yards apart on a gentle slope that rises 
northward to steep hills. One spring seeps from beneath a ledge of 
tuffaceous material. The other issues in a small excavation and 
forms a pool behind a cement dam. Each spring yields perhaps one- 
half gallon a minute of water of good quality. 

The hills north of these springs are com23osed partly of volcanic 
material, and the water seems to issue from a porous tuffaceous 
layer. These springs, however, like Willow Springs (Kern 22, p. 318), 
which have been described among the artesian springs, issue at the 
upper edge of a gentle slope that lies between a flat valley and steep 
hills, and the water may rise along a small fault that borders the valley. 

SPRINGS ON TEMBLOR RANCH (KERN 4). 

In the Coast Ranges that lie along the southwest side of San Joa- 
quin Valley there are a number of perennial springs that resemble in 
general character those in the southeastern part of the State, for they 
are in an arid region, are of small flow, and are of importance mainly 
because they form watering places. Those which are in the eastern 
portion of San Luis Obispo County and the western portion of Kern 
County have been of value as watering places for range cattle as weU 
as for travelers, however, so have been more often used than those 
in the southeastern desert region. The water of most of them is 
notably brackish or bitter, and a number of them are also sulphureted. 
One strongly sulphureted spring (San Luis Obispo 12, p. 277), that is 
used to supply cattle-watering troughs, has been described among 
the sulphur springs. Springs that rise on the Temblor ranch, about 
12 miles northwest of McKittrick, yield a supply of water that is 
sufficient for a smaU amount of irrigation. The water is not of very 
good quahty, however, being noticeably hard. 

THOMPSON SPRING (SAN LUIS OBISPO 6). 

Thompson Spring is in Carrizo Plam, westward across the Temblor 
Range from McKittrick. The spring rises in a curbed pool about 
8 feet square and 6 feet deep, at the base of a knoU of clay and 
gravel. It yields about 2 gallons a minute of shghtly brackish water, 
which is piped to a cattle trough near by. Two smaller springs are 



MINOR PERENNIAL SPRINGS. 355 

situated respectively about one-half niile and 1 mile west of it, on 
the Hubbard ranch. 

SPRINGS ON McALESTER RANCH (KERN 3). 

The McAlester ranch is supplied with water by springs of consider- 
able flow. Theu' yield has not been used for irrigation, however, for 
like other ranches in the region, the McAlester ranch is devoted almost 
entirely to stock raising. The springs are hence of importance mainly 
as furnishing a watering place for range animals. 

SPRINGS ON STILL RANCH (EIJRN 2). 

The Still ranch, at which Annette post office is situated, is suppHed 
by springs that yield a considerable flow of water of fair quahty. 
This water has furnished a domestic supply and has also been used 
in irrigating a vegetable garden. 

A number of other springs in this region have not been used or im- 
proved to notable extent and are hence mentioned among the peren- 
nial springs that are less well known. 

MUD SPRING (ALAMEDA 4). 

Mud Spring is near the road on the northeast side of the canyon of 
Arroyo Mocho, about 1^ miles in a direct line northwest of Menden- 
hall Springs. It issues a few yards above the road, in a shallow 
board-covered pool, and its water is piped to a watering trough at 
the roadside. It is of surface origin and apparently seeps from altered 
sandstones and sihceous shales of the Franciscan group. A similar 
spring issues near the roadside 4 miles farther southeast and supplies 
another watering trough. HaK a mile beyond this second spring a 
pit has been excavated at a small marshy place on the slope below 
the road and has furnished drinking water for the pupils of a public 
school near by. 

Another Mud Spring of similar character issues on the north side 
of the canyon of Trout Creek, 6^ miles directly south, but it is un- 
used. 

BANTA SPRING (SANTA CLARA 1). 

Banta Spring is near the northeastern border of Santa Clara 
County, about 13 miles south of Mud Spring (Alameda 4). It 
yields considerable water of fair quahty, and the locality has been 
occasionally used as a camping place by parties in the mountains. 

PEACHTREE SPRINGS (CONTRA COSTA 5). 

Peachtree Springs form a watering place for range stock, on the 
northwest slope of Mount Diablo. They are said to be named from 
a peach tree that formerly grew near one of them. The water, 



356 SPEINGS OP CALIFORNIA. 

which issues in two small marshy areas about 100 yards apart, comes 
from the Franciscan group of rocks that form the higher slopes of 
the mountain. Very little water flows from the springs, but they 
could probably be made to yield 8 or 10 gallons a minute. 

CHAPARRAL SPRING (CONTRA COSTA 6). 

A few small springs in the hills north of Mount Diablo are used to 
supply water troughs for cattle. One of the chief of these is Chaparral 
Spring, whose water issues in a small pool on the side of a ravine 3 
miles southeast of Clayton and is piped a few yards to a trough. The 
water seeps from a bank of crushed shales that dip nearly vertically. 
It is of good quality, but the flow is very small. A similar spring in 
another ravine half a mile southeastward also supphes a watering 
trough. 

PURITY SPRING (MARIN 4). 

Pmity Spring is situated on the slopes near Sausahto, on the 
northern side of San Pablo Bay. It yields a considerable flow of 
water that is not notably mineralized. For a number of years it 
has f lu-nished part of the municipal water supply and the water has 
also been bottled, under several names, for table use. 

SPRINGS AT VETERANS' HOME (NAPA 11). 

The main supply of water for the Veterans' Home near Yount- 
ville is obtained from a spring on the adjacent hiUside. This spring 
is about a quarter of a mile southwest of and 200 feet above the 
principal buildings, at a point where there was originally a small 
flow. The water now rises in an excavation about 10 feet wide, 25 
feet long, and 1 or 2 feet deep within a spring house. Five holes 2 
inches in diameter and 10 to 25 feet deep were drilled in the bottom 
of the basin that was formed, and the yield of water is said to have 
been increased by this means from a total flow of 7,000 gallons a day 
to one of 24,000 gallons (from about 5 to 17 gallons a minute). The 
water is piped to a reservoir near by and thence to the grounds of 
the institution. There is a small amount of the iron-secreting 
Crenothrix in the basin at the springs, and the water is faintly sul- 
phureted but of good quahty. 

Another spring issues in an excavation at the side of a small creek 
about 300 yards down the slope from the main spring. It yields 
about 4 gallons a minute and supplies a watering trough a few yards 
away. The basin at this spring also contains a small amount of 
brown iron-colored material. 

These springs issue from porous tuff aceous layers in rhyohtic lava 
that covers the slopes along this part of Napa Valley. 



MINOR PERENNIAL SPRINGS. 



357 



CRYSTAL SPRING (NAPA 6). 

Crystal Spring is on the grounds of the St. Helena Sanitarium, 
which is in the hills on the eastern side of Napa Valley, 3 miles north 
of St. Helena. The water issues in a small adit on the hillside 100 
yards southeast of the hotel and forms a part of the domestic supply. 
Its flow varies somewhat with the season, and in the summer of 
1909 it was said to have decreased to nearly one-half its former flow 
of 12,000 gallons a day. The normal summer flow is said to be about 
10,000 gallons a day (7 gallons a minute). The following partial 
analysis shows that the water is but slightly mineralized and is 
essentially secondary alkaline in character. 

Partial analysis of water from Crystal Spring, Napa County, Cal. 
[Analyst, E. W. Hilgard. Authority, owner of spring. Constituents are in parts per million.] 



Properties of reaction: 

Primary salinity 

Secondary salinity 

Tertiary salinity 

Primary alkalinity 

Secondary alkalinity 

Tertiary alkalinity 

Constituents 

Sodium (Na) 

Potassium ( K) 

Calcium (Ca) 

Magnesium (Mg) 

Sulphate (SO4) 

Chloride (CH 

Carbonate (CO3) 

Organic matter and combined water 

Silica (Si02) 




The water issues from lava which is similar to the material at the 
springs of the Yountville Veterans' Home. 

Other smaller springs on the higher slopes also furnish part of the 
water supply of the sanitarium. A similar spring that issues at the 
Pacific College, a few miles to the northeast, is reported to yield 
216,000 gallons a day (150 gallons a minute). 

GIFFORD SPRINGS (LAKE 47). 

In the mountainous portions of southern Lake County there are a 
few cool perennial springs, several of which have been improved for 
domestic and garden supplies. Gifford Springs are about 10 miles by 
road northwest of Middletown. and \\ miles east of the stage road, on 
a small mountain ranch. - Several years prior to 1910 the property 
was opened to the public as a mountain resort. The water issues at 
several points from lava slopes near a small creek which derives its 
supply mainly from springs beside its channel. Two small springs 



358 SPEINGS OF CALIFORNIA. 

in banks near the creek have been improved, one for a domestic 
supply and the other as a small drinking spring. The water is locally 
believed to contain considerable iron, and the presence of this mineral 
is indicated by rust-colored vegetable growths as well as by the red, 
iron-stained color of tiie lava. In the summer of 1910, which followed 
a season of unusually low rainfall, the two improved springs yielded 
only 3 or 4 gallons a minute, whereas the creek carried perhaps ten 
times as much, but in seasons of more plentiful precipitation the 
yield of the springs, as well as the flow of the creek, is much larger. 

SPRINGS AT BASE OF MOUNT HANNAH (LAKE 48). 

Cool fresh-water springs that yield perhaps 75 gallons a minute 
issue at the southeast base of Mount Hannah and supply water for 
irrigation and other uses on a small dairy ranch. Like the springs on 
the Gifford ranch, those of Mount Hannah come from lava slopes and 
seem to be directly dependent on the annual precipitation for their 
supply. 

In connection with these cold fresh-water springs on the Gifford 
ranch and Mount Hannah, it is of interest to note that no such 
springs are found on Mount Konocti, which lies at the edge of Clear 
Lake and overshadows Soda Bay. 

SPRINGS SOUTHWEST OF CHALK MOUNTAIN (LAKE 28). 

On the eastern side of Clear Lake and about 1 J miles southwest of 
Chalk Mountain, there are several small areas in which basaltic lava 
overlies the altered mariae sediments that cover a large part of the 
region. At the northern border of one of the largest of these lava 
areas, which forms a hill or ridge, cool fresh water issues at two or 
three places. The supply from the main springs, which yield per- 
haps 75 gallons a miaute, has been collected in a ditch and used for 
irrigation. These springs are of interest both because of their eco- 
nomic value and because spriags of this character are not common in 
Lake County. Their position at the northern border of the lava area 
is of geologic interest, as is also their proximity to Quigley Soda 
Springs (Lake 27, p. 195), which issue within a quarter of a mile of 
the fresh-water springs. 

LYONS SPRINGS (LAKE 22). 

A supply of water for domestic u.«e is furnished by springs at the 
home of Mrs. J. H. Lyons, on the hillside overlooking Clear Lake, 6 
miles north of Lakeport. The water issues along the side of a swale 
and forms a small marshy area a short distance back of the house. A 
part of it is lifted into a storage tank by a hydraulic ram. The water 
seems to be of surface origin and to be supplied by the precipitation 



MINOR PERENNIAL SPRINGS. 359 

on the neighboring slopes, but springs of this <'haracter are not com- 
mon in the hills of this region. 

ALDER SPRINGS (GLENN 1). 

Aider Springs are among the few perennial springs of palatable 
water in Glenn Colmt3^ They are situated about 40 miles by road 
north of west from Willows. Although they are only mountain 
springs of small flow, the locality has long been used as a summer 
camping place and hence the springs are well known to many resi- 
dents of the county. 

PERENNIAL SPRINGS THAT ARE LESS WELL KNOWN. 

In addition to the perennial springs that have been separately 
described and that are shown on Plate I (in pocket), there are many 
that are known locally as watering places on roads or trails, and still 
others that are utilized for domestic supply and garden irrigation. 
These minor springs are not indicated on the map (PI. I), but some 
of them are here mentioned with such information as is available. 

In the northeastern part of the State, on the stage road between 
Alturas and Cedarville, about 6 miles northwest of the latter place, 
there is a spring which yields 2 or 3 gallons a minute of water about 
47° in temperature. It is in a ravine at a bend m the mountain 
gi'ade a few yards from the roadside and furnishes a convenient 
watermg place. 

On the south side of Pit River, beside the stage road 2^ miles 
southwest of Canby or 27 miles south of west from Alturas, there 
is a rock- walled drinking spring which yields 8 or 1 gallons a minute 
of water 59° in temperature. A pipe leads from the spring down the 
slope to a horse trough at the roadside 50 yards away. 

Several perennial springs of considerable flow issue in the lava 
beds south of Tule or Rhett Lake at the north end of the State, but 
as they are in an uninhabited region they are little kno\\ai. One 
spring of this character lies near the west end of Medicine or Crystal 
Lake, which is 55 miles in a direct line west of Alturas, and another 
is situated at the north base of Black Fox Mountain, 1 7 miles to the 
southwest. 

In the Lassen Peak region, in addition to the large perennial 
springs, several of which have been described among the large cold 
springs, there are several minor springs that are of local unportance 
in this part of the State. One of these is Burney Spring which 
issues beside a road along the southern base of Burney Butte. It 
yields perhaps 10 gallons a minute and affords a watering place for 
range cattle as well as for travelers. Moon Springs, which lie farther 
east, about 10 miles south of east from Rising River (Shasta 11, 
p. 328), have been improved by piping their flow to troughs for water- 



360 SPEINGS OP CALIFORNIA. 

ing range stock. There are two springs at the locality, but their 
yield is small. Coyote Spring is about 12 miles south of Moon 
Springs and like them it yields a small amount of water and is used 
by range stock. Tadpole Spring is on the southwestern slopes of 
Lassen Peak beside the stage road, 3 miles east of Paynes Creek 
post office. It yields a slight flow that is piped to a roadside watering 
trough, 100 yards to the northeast, and to a house near by for domestic 
use. The water issues from the tuffaceous material known as the 
Tuscan tuff, the supply probably being derived from water that col- 
lects in a porous layer of the material. Springs are not plentiful in the 
lower slopes of the lava area that surrounds Lassen Peak, so those 
which exist are of local importance. On the higher slopes, however, 
water is more plentiful and the presence of small springs of fresh 
water is of less importance. 

In Plumas County, on the stage road between Quincy and Green- 
ville, there are a number of springs that supply roadside watering 
troughs. Their waters issue from slate and shale along the canyons 
of Spanish and Indian creeks, and they yield flows of about 1 to 10 
gallons a minute. Eight springs of cold nonmineral water that supply 
drinking pools or horse troughs were counted at the roadside along the 
canyons of these creeks. A number of cold springs issue in meadow- 
land in Grizzly VaUey, about 12 miles northwest of Beckwith, and 
furnish a considerable part of the flow of Big Grizzly Creek. 

The lower portions of the western slopes of the Sierra contain 
relatively few perennial springs. Some of these surface springs 
were early made use of, however, by miners who were working gold 
placer gravels and ledges, and small settlements were formed near 
them. Forest Spring, which is 3 miles south of Nevada City, and 
Indian Springs, which are 8 miles southwest of the same town, lent 
their names to mining settlements. There are also several perennial 
springs in Eldorado County at places where mining camps were built 
up in the early days, but the springs are not now of great importance. 
Among these are Shingle, Mud, and Diamond springs, near the rail- 
road between Sacramento and PlacerviUe. Several other springs 
afford watering places on a road between PlacerviUe and Silver Lake, 
which is a small water body in the northeastern corner of Amador 
County. Among them are Caple, Camp, Leek, and Tragedy springs, 
which are respectively about 26, 30, 40, and 47 miles by road eastward 
from PlacerviUe. AU yield cold water of good quality but are of 
small flow. A few springs near the boundary between Eldorado and 
Amador counties are also of some importance as watering places. 
Among these are Marble, Antelope, and Mud springs, which are, 
in direct lines, respectively 22, 28, and 35 miles east of Latrobe station 
on the raihoad to PlacerviUe. 



MINOR PERENNIAL SPRINGS, 3()1 

Mountain Springs, G miles west of Jackson in Amador County, and 
Valley Springs, at the terminus of the railroad 10 miles west of 
San Anflreas in Calaveras County, are at small settlements. There 
are also saline springs near the latter place, which have abeady been 
described. Cottage Spring, 5 miles northeast of Valley Springs, 
has been locally used as a water supply. Another Cottage Spring 
and Black Spring and Hermit Spring are near the road that runs 
northward from the north grove of the Calaveras big trees, in north- 
eastern Calaveras County. 

Colfax Spring, which is on the south edge of Tuolumne County, 25 
miles in a direct line southeast of Sonora, has given its name to a small 
settlement. Gold Spring, 7 miles north of Sonora, and Cold Spring, 
30 miles northeast of the same town, are locally known. 

Fremont Spring, which is on the southeast slope of Bullion Moun- 
tains, 30 miles in a direct line northeast of Merced, is known to the 
miners of the locality. In the higher Sierra east of Merced there are 
a few small perennial springs, among the principal ones being Cold 
Springs, between Mariposa and the Mariposa Grove of big trees. A 
few larger ones in the Sierra have been previously described. 

Numerous cool springs of perennial flow issue along the north- 
western border of Mono Valley, in the eastern part of the State. 
Several of them afford watering places for range cattle and horses, 
and a few irrigate small meadows, but they have not been efficiently 
developed. One that rises on the southern side of Mono Lake a short 
distance from the water's edge was formerly known as Blairs Spring. 
The water is noticeably calcic, but it has long been used as a drinking 
spring. Other small springs rise in the lake and several of them issue 
from domes or crags of calcareous tufa that are built up from the lake 
bottom. These springs have been mentioned in the description of 
Mono Basin Warm Springs (Mono 8, p. 145), and an analysis of water 
from one of them is tabulated wath that of water from the warm 
springs. 

In the higher portions of the southern Sierra a few small springs 
form drinking places beside mountain traUs. Among them are Windy 
Springs, which are on a tributary of South Fork of Kern River, about 
13 miles in a direct line southwest of former Haiwee stage station 
(Inyo 26, p. 339) ; Boulder Spring, which is 18 miles by trail southeast 
of Onyx post office; and Bird Spring, which is 20 miles by trail 
southeast of Weldon post office and 6 miles in a direct line west of 
Boulder Spring. 

Along the arid southeastern portion of tlie Sierra, southward from 
Haiwee to Mohave, there are very few perennial springs, though 
seepage or underflow in Red Rock Canyon and farther south, at Water 
Station (Kern 21, p. 341) , yields a fairly dependable supply. South of 
Mohave, in the mountains bordering Antelope Valley, in whose basin 



362 SPEINGS OF CALIFORNIA. 

lie the towns of Lancaster and Rosamond, there are a few permanent 
springs. Antelope, Love joy, and Moody spruigs are three which issue 
near buttes that rise in the valley proper and have been described as 
probably due to underflow water that is forced to the surface by the 
outcropping bedrock.^ Several other springs that issue from the 
slopes above the valley have been used for domestic supply and for 
cattle, and one group has even been developed and piped to the 
settlement of Neenach, in the west end of the valley for a town supply.^ 

In the ranges of the desert eastern and southeastern portions of the 
State there are many springs of shght flow that are used as watering 
places by prospectors, but most of them are less important than those 
which are indicated on Plate I (in pocket) and which have been 
separately described. A number are here mentioned, however, 
because they are really more important than many larger springs in 
other parts of the State.^ 

On the slopes of the White Mountains and Inyo Mountains, along 
the east side of Owens Valley, a number of small springs that would 
receive little notice in a better-watered region are of importance to 
prospectors and others who have occasion to cross these ranges. 
Among them are Cedar, Coldwater, Black Canyon, and Goat springs, 
beside or near roads leading eastward from the town of Bishop into 
Nevada, and Graham and McMurray springs on the slopes a few miles 
east of Alvord. 

Santa Anita, Willow, and Coyote springs are on the slopes of the 
Inyo Mountains, eastward from Independence, and are respectively 
4 miles northwest, 5 miles south, and 9 miles south from Barrel 
Springs (Inyo 9, p. 338). Like the latter they furnish small supplies 
of water to prospectors in the region. 

In the Coso Range, which lies southeast of Owens Lake, there 
are a number of small springs that are away from the traveled roads 
and are known mainly to prospectors. Among these are WiUow 
Springs, about 4 miles northeast of Darwin post office, and a spring 
in the pass between the Coso and the Argus ranges, about 12 miles 
southward from Darwin. A third spring, which is on the eastern 
slope of the mountains, about 10 miles farther south in the same 
pass, also yields a small amount of water of good quality. All three 
of these springs have long been used and are marked by camp litter. 

In the Panamint Range there are a number of springs of less im- 
portance than those in this range which have already been described. 
Rest Spring and Burro Spring are situated about 1| miles apart, on 

1 Johnson, H. R., AVater resources of the Antelope Valley, California: U. S. Geol. Survey Water-Supply 
Paper 278, pp. 52-53, 1911. 

2 Idem, pp. 54, 55. 

3 Most of the springs in the southeastern part of the State that are mentioned are described more fully 
by W. C. Mendenhall in Some desert watering places in southeastern CaUfornia and southwestern Nevada: 
V. S. Geol. Survey Water-Supply Paper 224. 



MINOR PERENNIAL SPRINGS. 363 

a trail that loads northeastward from Koolor. Thoy arc respectively 
oil tlie western and the eastern sides of tlie Panamint Range, directly 
east of Independonce. Each furnishes about 3 barrels a day (half 
a pmt a minute) of good water. Goldbelt Sprhig is about 15 miles 
south of Rest Sprmg and is near the junction of trails that load from 
it northward along the range and eastward to Death Valley. It yields 
perhaps 20 barrels a day (half a gallon a minute). 

Several springs of mmor importance issue along the eastern side of 
Death Valley and in the mountain slopes that border it. Grapevine 
Springs are about 3 miles by trail west of the Staininger or Grapevine 
ranch (Inyo 11, p. 342). They yield a supply of good water but are 
away froih the main-traveled routes. Mesquite Spring is 6 miles 
farther south, m the east bank of the wash of Death VaUoy, and near 
the road. Triangle Sprmg is also near the road that leads southeast- 
ward through Death Valley. It issues m a clay bank near a clump 
of mesquite, about 25 miles southeast of Mesquite Springs. Tule 
Sprmg and Willow Spring are m the southern portion of the Grape- 
vme Mountains, 3 or 4 miles westward from Daylight Spring (Inyo 
13, p. 342), and about 3 miles apart, near a trail between Death Valley 
and Bullfrog, Nov. Fountain Springs are at the base of a butte on 
the eastern border of Death Valley and about 6 miles north of the 
Furnace Creek ranch (Inyo 20, p. 320). They yield a small water 
supply for prospectors in the near-by mountains. 

There is another Tule Spring beside the road about 6 miles east of 
Tecopa railroad station and 2 or 3 miles southeast of Resting Springs 
(Inyo 34, p. 319), near the southern border of the county. It yields 
a small supply of water of fair quality and has been boarded over to 
protect it from cattle. 

There are a few perennial sprmgs of little importance in the moun- 
tains of the Randsburg mming district. WiUow Springs, on the road 
10 miles north of Randsburg, are of seepage flow and have been little 
used since an ample water supply was obtained in a weU a mile to the 
northwest. Bedrock Spring, which is on the north side of Klmker 
Mountain, 10 miles northeast of Randsburg, yields a small water 
supply, but it is on a road that has not been much used. Squaw 
Spring is 5 miles east of Randsburg. It has no appreciable flow 
and is used mainly by prospectors. 

A few springs in the northeastern corner of San Bernardino County 
are of local value to prospectore in the region. Horse Spring, on the 
eastern side of Kingston Range, jnelds good water from shale or 
slate. Coyote Holes are about 12 miles to the south or southwest, 
near the divide between Kingston Range and Shadow Mountains. 
Their water is brackish, and better w^ater can be obtained at Kingston 
Springs, which are about 2 miles farther south. Cunningham Spring 
is at the northeast base of Shadow Mountains and is 6 miles south- 



364 SPEINGS OP CALIPOENIA. 

east of Coyote Holes, and Pachanca or Pachalka Springs are 5 or 6 
miles eastward, at the base of Clark Mountain. 

In the mountains near the eastern border of the State, in the min- 
ing regions of Ivanpah, Leastalk, and Vontrigger, numerous small 
perennial springs are of great importance to the mining industry. 
Several of these springs have already been specifically described,' 
others, which are of nearly equal importance, are Willow and Malpais 
springs, in the eastern portion of the New York Mountains, and 
Hackberry Spring farther southward, in the mountain of the same 
name. All these springs have been piped some distance to mines or 
to water troughs. 

Harpers mining camps are two camps in the southern end of the 
Avawatz Mountains, about 12 and 15 miles, respectively, northwest of 
Silver Lake raiboad station. Water has been obtained at the southern 
camp by tunneling into granite. At the northern camp an ample 
supply issues from beneath limestone. 

Goleta Spring is at the southeast base of Fremont Peak and about 
25 miles southeast of Randsburg, on an old road to Barstow. The 
spring was visited by Fremont on his last homeward journey across 
Mohave Desert, but there has been little travel past it during recent 
years and it has become of little importance. 

Indian Spring is in the mountains about 25 miles in a direct line 
north of Daggett. It supphes a few gold miners who work dry placers 
in the locality, but it is unimportant to the desert traveler. 

Canyon Spring is 6 miles east of Paradise Springs (San Bernardino 
9, p. 52), and is beside a road that leads northward past GarHc Spring 
(San Bernardino 10, p. 303). This route of travel has been seldom 
used diu"ing recent years, so the spring has become of httle importance. 

Barrel Spring was formerly a well-known watering place near the 
western border of Soda Lake and 2 or 3 miles north of the crossing of 
the Salt Lake and the Tonopah & Tidewater railroads. Since the 
construction of these lines of travel the spring has been Httle used. 

Marl Springs are 9 miles southwest of Cima railroad station and 
about 12 miles south of Kessler Springs (San Bernardino 15, p. 344), 
on a slightly used road that connects the two watering places. Like 
Kessler Springs the place has been used as a camp by prospectors. 

There are at least three springs that are used by prospectors near 
Granite Mountain, which is about 25 miles north of east from Lud- 
low: Cottonwood Springs, near the northern end of the mountain, in 
the pass between it and the Providence Mountains, and on a road 
that leads to Kelso raihoad station, 15 miles north; Cove Springs, 
near the road and 6 miles farther south, at the southeast edge of the 
mountain; and Willow Springs, at the southwest end of the mountain 
and 5 miles by trail west of Cove Springs. All three groups of springs 
yield smaU amounts of water of good quality. 



MINOR PERENNIAL SPRINGS. 365 

Bonanza Springs form a good watering place on the south side of 
Oipper Mountain, which is southeast of Granite Mountain but north- 
west of the Salt Lake railroad. Still farther southeast Old Woman 
Springs yield a considerable flow in a canyon at the northeast end of 
a mountain of tlie same name. Other Old Woman Springs (San 
Bernardino 27, p. 316), which are about 90 miles farther west, have 
been described among the artesian springs. Sunflower Springs, 8 
or 10 miles north of the springs on Old Woman Mountain, form a 
watering place for range cattle. On the western side of the mountain, 
about 8 miles southeast of Old Woman Springs, there is a spring of 
good water near the ruins of a mining camp, and at the southern end 
of the mountain there are other small springs that are used by 
prospectors. 

Considerable water issues along the course of Mohave River near 
Victorville, apparently as springs of surface or possibly alluvial arte- 
sian origin. Little direct use is made of them, as more convenient 
water supplies are obtained from the river and from wells. 

Kanes Spring is 9 miles southeast of Newberry Springs (San Ber- 
nardino 20, p. 317), at the eastern base of Kane Mountain, on a road 
to Victorville. Its water is of good quality, and it forms a convenient 
stoppmg place for travelers. Koehn or Kane Springs form another 
watering place of similar name (Kern 20, p. 340). 

About 8 miles southeast of Kanes Spring, at the eastern side of 
Bessemer Mountain, there is another small spring. Its water is 
slightly brackish, but it has been used by miners who have prospected 
the iron deposits in the adjacent mountain. 

A number of small sj^rings issue in the northern portion of the 
San Bernardino Mountains. Rock Springs are in a canyon near the 
northern base of these mountains, about 6 miles east of Mohave River. 
They form a small watering place on a road between Cactus Flat 
(San Bernardino 30, p. 347) and Victorville. Rock Corral Spring is 
at the northeastern edge of San Bernardino Mountains and about 
10 miles southeast of Old Woman Springs (San Bernardino 27, p. 
316). The place is marked by a rock corral and the water is plentiful 
and of good quality. Twohole Spring issues from a 10-foot tunnel 
in a granite bank, about a mile east of the road and 6 miles north- 
west of Rock Corral Spring. It yields about 1 gallon a minute 
and has been used as a watering place for cattle. Terrace Springs, 
5 miles farther west, also furnish a small supply that has been 
used for cattle watering. Viscera Spring is in a ravine that is 
tributary to Rattlesnake Canyon; it is about 7 miles southward by 
road from Twohole Spring but three-quarters of a mile from the 
main road. It is shaded by a scrubby willow tree and yields a very 
small flow of water that deposits considerable iron. About Ih miles 
southeast of it another small spring rises beside the road and near 



366 SPRINGS OF CALIFORNIA. 

tlie head of Rattlesnake Canyon. Saddlerock Spring forms a small 
watering hole for cattle in a canyon about 7J miles in a direct line 
east of Viscera Spring and twice as far southeast of Old Woman 
Springs. Burns Spring yields a small amount of good drinking 
water beside the road in the canyon of the same name 5 miles south- 
west of Saddlerock Spring; it seeps from gray decomposed granite 
along the creek side, from small holes dug in the bank for a distance 
of about 15 yards. Springs in the canyon of Pipes Creek, 3 miles 
south of Burns Spring, yield a small flow, which is piped some distance 
down the canyon to the ranch house known as The Pipes and also 
a quarter of a mile farther east to a small reservoir that serves as 
a cattle-watering place. Chaparrosa Springs are in a ravine about 
3 miles south of The Pipes. Two springs, 100 yards apart, in this 
ravine furnish seeping flows from basins dug in the bank of the 
drainage channel and have been used by cattle as watering places. 

There are also a few minor springs in the southeastern extension 
of San Bernardino Mountains. Stubby Springs, which are on the 
western slope of the range, 18 miles north of Indio, are locally known. 
Lost Horse Spring is about 8 miles farther eastward, near the eastern 
base of the range. At one time it supplied a 2-stamp mill near by. 

McCoy Spring forms a watering place on the west side of Ironwood 
Mountains, on a road between the Colorado Desert and Ehrenberg, 
Ariz. The spring yields only about 4 barrels a day (less than one 
pint a minute), but the water is of good quality. 

Two groups of springs in the Palo Verde Mountains, in the southeast 
corner of Riverside County, are of local value as watering places. 
One group is at the base of a westward extension of the mountains, 
beside a wagon road between the Colorado Desert and Ehrenberg, 
and is 5 or 6 miles west of Mule Springs (Riverside 23, p. 348); the 
other is at the northeast side of the Palo Verde Mountains and forms 
a watering place for cattle. 

A few springs form minor watering places in the mountains on the 
west side of the Colorado Desert. Among these are Dos Palmas 
Spring, 14 miles in a direct line southwest of Indio; Asbestos and 
Potrero springs, which are respectively 3 miles west and 5 miles 
northwest of Dos Palmas Spring; and Cactus, Virgin, and Agua Alta 
springs, which are between 5 and 10 miles to the south. Most of 
these springs have been used as sources of water by prospectors in 
the region. Seventeen Palms Springs are on a road from the mining 
settlement of Julian northeastward to the desert and are 12 miles 
byroad eastward from Borego Spring (San Diego 6, p. 349). The 
water is of fair quality when the springs are kept cleaned out, but as 
the road is seldom traveled the springs are usually choked by sand 
and weeds and the water is alkaline. Zacaton Spring is on the south 
side of the same road, about 5 miles farther east. Mountain Palm 



MINOR PERENNIAL SPRINGS. 307 

Springs are 4 or 5 miles southwest of the Mason ranch (San Diei^o 1 0, 
p. 349), and about the same distance from the main wagon road, but 
they yield a fair supply of cool water and make a good camping place. 

On the western slopes of the southern Coast Ranges a few perennial 
spiings form roadside drinking ])ools, or pools that are known to 
hunters. Dog Spring is in a direct line about 12 miles northeast of 
San Diego, and Tule Spring is 13 miles eastward from the railroad 
terminus at Foster. Cold S])ring, on the stage road between Descanso 
and Cuyamaca, yields perhaps 5 gallons a minute of water 55° in 
temperature and forms a drinking pool at the roadside. Durasnitos 
Spring furnishes a small supply about 4 miles southwest of Ramona 
or 3 miles northeast of Bradley Spring (San Diego 7, p. 350). Drip- 
ping Spring and Sawyer Spring are in canyons tributary to Temecula 
Creek and are respectively about 9 miles and 13 miles in direct 
Hnes east of Temecula, in southwestern Riverside County. They 
yield small flows of little importance. 

In a canyon 3 miles north of Arrowhead Hot Springs (San Bernar- 
dino 36, p. 32), there is a cold spring of considerable size, and near 
the hotel is a cold spring (Fuente Frio), whose analysis is given with 
those of the hot waters. Another small cold spring issues several 
miles to the northwest, 3 miles south of the warm spring in Lytle 
Canyon (San Bernardino 34, p. 35). 

Crystal Spring, on Mount Lowe in the San Gabriel Mountains, 20 
miles northeast of Los Angeles, yields cold pure water that was at 
one time bottled for table use. 

In the mountains 8 or 10 miles northwest of Santa ]\Ionica, which 
is on the coast west of Los Angeles, are several minor springs that 
form small watering places for range stock. Water is scarce in these 
mountains, however, and as the main perennial springs are sul- 
phureted they have been described among the sulphur springs. 

Several localities of perennial springs in the Coast Ranges along the 
southwest side of San Joaquin Valley have been previously men- 
tioned and are indicated on Plate I (in pocket). Springs of similar 
character issue at other places in this arid region. Pataroma Spring, 
11 miles in a direct line south of west from Maricopa, furnishes a small 
cattle-watering supply. Goat Spring, which is about 2 miles south 
of the sulphur spring in Carrizo Plain (San Luis Obispo 12, p. 277) 
yields slightly bitter or salty water that is used to some extent 
by cattle. Five willow Spring, which is 2 J miles northwest of the 
sulphur spring, yields water of fair quality for stock use, and a 
similar spring 2 miles southwest of Painted Rock ranch, or 9 miles 
northwest of the sulphur spring, also yields a small flow. Mustang 
Spring furnishes a small watering place beside a road, 4 miles west 
of north from Thompson Spring (San Luis Obispo 6, p. 354), but in 
summer it becomes nearly dry. Carnaza Spring, on the creek of the 



368 SPRINGS OF CALIF OKNIA, 

same name, 10 miles northwest of Thompson Spring, yields a larger 
supply than m.ost springs of the region, as it forms a stream of perhaps 
10 to 15 gallons a minute. Its water is of good quality, but as the 
spring is not on a road it has been used mainly by cattle. A small 
spring on the San Juan ranch, about 10 miles west of Thompson 
Spring, yields water that is noticeably sulphureted, but the spring is 
not distinctive in this respect, for most of the water of this region is 
distinctly sulphureted. Crocker Spring, on the creek of the. same 
name, about 6 miles west of south of McKittrick, yields a small flow 
of mildly sulphureted water; it has furnished a camp supply for 
stockmen. Frazer Spring, 5 miles northwest of McKittrick, is an 
old roadside watering place, and Sheep Springs, 2^ miles west of 
Frazer Spring, yield small stock-watering supplies. Carneros Spring, 
6 miles northwest of the Temblor ranch (Kern 4, p. 354), in a tributary 
to Carneros Canyon, yields fair water. Walnut Spring and Antelope 
Spring are about one-half mile apart and 8 miles in a direct line 
northward from Thompson Spring. The former yields a good flow 
of water of fair quality; the latter is of smaller flow and is less impor- 
tant. Napoleon Spring yields slightly bitter water in a tributary of 
Cedar Canyon, at a point about 2|- miles northwest of Antelope 
Spring. It is about 1 mile from a road, but it is well known to stock- 
men of the region. Aido Spring is on the north side of Antelope 
Valley and 6 miles in a direct line northeast of the Still ranch (Kern 
2, p. 355). Its name was coined from the initials of the phrase "all 
in, down and out," by two oil prospectors who foimd it one hot sum- 
mer day. It yields a small amount of water of fair quality. A spring 
in Cottonwood Canyon, 5 miles farther north, also yields a small 
quantity of fair water. Alamo Solo (Lone Poplar) Spring is about 4 
miles north of the salt spring near Antelope Valley (Kern 1, p. 301) 
and yields a small water supply in the northeast end of the Devils 
Den oil district. 

Farther northwest, in the Coalinga region, there are very few springs 
of even seeping flow, but in the vicinity of Mercey Hot Springs 
(Fresno 8, p. 78) there are a few of minor importance on the slopes 
tributary to Little Panoche Creek. Among the principal springs in 
this region, however, are probably those a few miles farther north at 
Laguna Seca ranch, which is about 20 miles southwest of Dos Palos, 
and Piedra Azul Spring, Carrisalito Spring, and the spring at Arbu- 
ruas, the three last mentioned being on the Carrisalitos ranch, a few 
mUss west of the Laguna Seca ranch. 

There are a few perennial springs of minor importance in the 
ranges of northwestern San Luis Obispo and southwestern Monterey 
counties. Among them is Round Spring, which is in the Los Burros 
mining district and is 6 miles from Nacimiento River. A few other 



MINOR PERENNIAL SPRINGS. 369 

springs peld domestic supplies or form watering places for cattle in 
tliis portion of the Coast Ranges. 

A domestic supply of good water is obtained at Tassajara Hot 
Springs (Monterey 3, p. 57), from cold springs in a canyon near the 
hotel. An analysis of a cold iron spring at this place has been given 
with the analyses of the hot springs. 

In Santa Clara County a small spring of cool water forms a roadside 
drinking place between Gilroy and Gilroy Hot Spring (Santa Clara 
9, p. 79), and larger cool springs near this resort furnish a domestic 
water supply. 

Springs of considerable flow issue on the slopes 2 or 3 miles south 
of Alma railroad station, which is 12 miles southwest of San Jose. 
Similar springs form the water supply at a small mountain resort 
2 or 3 miles farther west, and several others in the locahty form 
roadside drinking springs. 

In the great interior valley of Cahfornia there are very few springs. 
On the eastern side of Sacramento Valley, near the base of the Sierra, 
however, there is an occasional small spring near a stream channel. 
Willow Spring, which is about 30 miles southeast of Sacramento, is 
one of these, and it is probably supphed by subsurface water from 
the slopes to the east. 

Numerous cool nonmineral springs of perennial flow exist in the 
abundantly watered portions of the Coast Ranges north of San Fran- 
cis© Bay, but as most of the mountainous country is sparsely inhab- 
ited, the springs are of little importance even on cattle ranges, for 
the many streams in the region furnish adequate watering places. 
A few of them form watering places along stage roads, however. 
Among those which are thus made use of the springs at Bell Springs 
station, near the northern border of Mendocino County, on the stage 
road 40 miles northward from vSherwood, are perhaps the best known. 

A few small springs in Lake County furnish roadside watering 
places. One spring that is about 4 miles south of Middletown, 
beside the road to Calistoga, issues from serpentine and yields per- 
haps 2 gallons a minute of water of good quahty. Another spring, 
about 2 miles farther south, also yielding about 2 gallons a minute, 
has been piped a short distance down the slope to a watering trough 
at the roadside. Tlu^ee-fourths of a mile west of Allen Springs (Lake 
11, p. 198) a slightly used road branches from the stage road, climbs 
southward across a divide, and thence descends into the valley of 
Wolf Creek. About a quarter of a mile southeast of its junction with 
the stage road a spring that yields about 2 gallons a minute of cool 
water of good quality issues from the road bank and forms a pleasant 
drinking spring. About 2^ miles beyond it, or a quarter of a mile 
35657°— wsp 338—15 24 



370 SPRINGS OF CALIFOENIA. 

north of the road summit and 25 yards from the road, there is another 
spring that has been improved by a joint of pipe and a half barrel 
so as to form a watering place. Both of these springs issue from 
crushed and altered sediments that constitute the greater part of the 
rocks in this region. 

On the road that leads from Bartlett Springs (Lake 9, p. 200) to 
Crab tree Springs (Lake 5, p. 106), about halfway between the two 
places, on the grade north of Twin Valleys, a spring that issues from 
altered sandstone and forms a welcome drinking pool yields about 3 
gallons a minute of good water. 

Candybucket Spring is thus locally known because a candy bucket 
was for some time kept near it for the use of teamsters in watering 
their teams and of automobihsts in replenishing their radiators. It 
issues at the side of the road between Stonyford and Fonts Springs 
(Colusa 3, p. 205), about 3 mUes east of the latter place and 100 yards 
north of the summit of the grade between the two places. It yields 
a summer flow of 2 or 3 gallons a minute, but the water issues from 
altered sediments near an area of serpentine and is not very good. 

Rattlesnake Spring is at the roadside about 6 miles east of Alder 
Springs (Glenn 1, p. 359). It yields a small flow that has been used as 
a roadside watering place, but it is of interest chiefly because water is 
not plentiful in the region. 

In the portions of the Coast Ranges that drain into northern 
Sacramento Valley water is much scarcer than it is farther southwest. 
Among the springs in the higher part of this region may be mentioned 
one on the northern side of Toms Head Mountain, about 10 miles 
northwest of Colyear Springs (Tehama 10, p. 266), and another near 
the county line, about 8 miles farther northwest. Near the summit 
of the range, 25 miles farther north, Kenshaw Spring issues about 6 
miles south of DeerHck Springs (Trinity 3, p. 261). A spring at the 
creek edge one-half mile south of DeerHck Springs is of interest be- 
cause of the coldness of its water, a temperature of 47° being recorded 
in summer. 

In the rugged portions of Humboldt County, back from the 
coast, there are several nonmineral springs, and a few that are 
better known issue in the less sparsely inhabited section along the 
larger streams. One of these springs is about 2 miles north of Mad 
River and 7 miles from the coast, and a larger one issues a mile east 
of Trinity River and 4 miles south of the northern border of the 
county. 

In Del Norte County, which is in the northwest corner of the State, 
there are at least four springs of notable flow in the drainage basin of 
Smith River. Two of these springs are on branches of the south fork 
of the river and are respectively about 17 miles southeast and 10 



TABULATED DATA. ' 371 

miles south of east of Ci-esceiit City; the third spring is about 8 miles 
east of this town; and the fourth is on the north fork of the river, 15 
miles northeast of the same place. 

TABULATED DATA. 

Table 1 contains an alphabetic list by counties of aU the springs 
whose locations are shown on the map, Plate I (in pocket) . The names 
of the owners of springs (so far as known) are given, and the approxi- 
mate distances by the usually traveled routes from the nearest rail- 
road station or from the principal town in the region. Many of the 
figures that give elevation, number of springs, temperature, and yield 
do not agree with figures previously published, but they were ob- 
tained mainly by personal observation and are beheved to be approx- 
imately coiTect. The column showing development or use gives the 
conditions noted during the period covered by the field examination 
These conditions vary somewhat from year to year, for commercially 
developed springs are occasionally abandoned and undeveloped springs 
are improved as resorts or for bottling water or other purposes, but 
the total number of springs is almost constant. 

Table 2 contains a list of the springs that were used during the 
period covered by the field examination either as permanent resorts or 
as camping places. It gives the distances from raiboad or supply 
points, and the capacity, open season, and improvements of resorts, 
these latter three factors being of course changeable. 



372 



SPEINGS OF CALIFORNIA. 



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376 



SPKINGS OF CALIFORNIA. 



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377 



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o»o o ooo o 

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ooo ooooo OOOOCO 



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378 



SPEINGS OF CALIFOENIA. 



flS 



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rt' ,-TcO THNrH rHrH{M"'i-rC<r 



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TABULATED DATA. 



379 



o « o 


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oo 
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380 



SPRINGS OF CALIFORNIA. 



n P 





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a'o.g 



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COrt rt M 



o o o o o lo oooo 
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, r-i OO TT .-t T-H Ol OOCNtH 



oo oo 
o o o >o 
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TABULATED DATA. 



381 



"g 5 -a o-S d 

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382 



SPRINGS OF CALIFOEISriA. 



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TABULATED DATA. 



383 



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5 ft 



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lO CS LO 0*0 

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384 



SPEINGS OF CALIFORNIA. 



^S 






6 o"g fl'g g^J 
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S-d 



ci IS d ts ® S fl 



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:no ooooO'Tti^^ ooo coo 
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o o o ^ ^ 



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OC^OiO(N»00 O C^l (M CN O GO (M 



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CC ^ 03 03 O <N 0"3 



OOOO 
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p. 



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03 O^ OWI-H 53 



TABULATED DATA. 



385 



aori 




■doj 


t 


5 ^ 




OS 


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gs.ge.s 

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g fig 



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397 



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398 



SPBINGS OF CALIFORNIA. 



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TABULATED DATA. 



399 



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400 



SPRINGS OF CALIFORNIA. 



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402 



SPBIFGS OP CALIFORNIA. 



■SB 



M 03 bcbe M 



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INDEX. 



A. 

Page. 

Adams Springs, description of 189-190 

Mtna. Springs, description of 156-159 

Ager, large cold springs near, description of . . . 331 
Agnew Meadows, carbonated spring at head 

of 238 

Agua Caliente Springs (San Diego County), 

description of 46 

Agua Caliente Springs (Sonoma County), de- 
scription of 113-114 

Agua Dulce Springs, description of 314 

Agua Tibia Springs, description of 47 

Aqua Vitae Mineral Well, description of 306 

Alameda County, list of springs in 372 

Alamo Bonito Springs, description of .'. . . 314 

Alder Springs, description of 359 

Alder Glen Springs, description of 166-167 

Algse at Tassajara Hot Springs, description of. 59-60 

varieties of, in springs 20-21 

AUiambra Springs, description of 293-294 

Alkaline waters, value of 27 

Alkalinity, grades of 23 

Allen Springs, description of 198-199 

Alpine County, spring in 372 

Alturas, artesian spring near, description of. 323-324 

Alum Rock Park Springs, description of 208-212 

Alum Spring, description of 197 

Aluminum, source of, in water 17 

Amedee Hot Springs, description of 127 

American River, Middle Fork of, sulphur 

spring on , description of 285 

North Fork of, salt springs on, descrip- 
tion of 300 

sulphur spring near, description of 285 

Ammonium radicle, scarcity of, in spring 

waters 19 

Analyses, conversion of 29-30 

sources of 28-29 

Analysis of water, methods of 15-16 

Anderson, Winslow, cited 26 

Anderson Springs, description of 89-91 

Antelope Valley, salt spring near, descrip- 
tion of 301 

Arab Spring, description of 339 

Arlington Springs, description of 229-230 

Arrowhead Hot Springs, analyses of 34 

description of 32-33, 35 

plate showing 32 

Arsenate, scarcity of, in spring waters 19 

Artesian springs, descriptions of 313-326 

Astorg Spring, description of 188-189 

Azule Mineral Spring, description of 212-214 



B. 

Page. 
Bailey Creek, artesian springs near, descrip- 
tion of 326 

Baker Mineral Spring, description of 173-174 

Baker Soda Spring, description of 193 

Baldwin Lake, warm spring at, description of 35 

Banes Soda Springs, description of 215 

Banner Spring, description of 337 

Banta Spring, description of 355 

Barrel Springs, description of 338 

Bartlett Springs, description of 200-201 

plate showing 200 

Bassett Hot Spring, description of 117 

Battle Creek Meadows, sulphur spring near 

head of, description of 283 

Bear Creek, carbonated spring on, descrip- 
tion of 203 

Bear River, sulphur spring on, description 

of 284-285 

Beaver Creek, carbonated spring on, descrip- 
tion of 217 

Bell Canyon, sulphur springs near, descrip- 
tion of 281 

Bennetts Wells, description of 343 

Benton Hot Spring, description of 136 

Beregin, source of, in spring waters 20 

Bertrand ranch springs, description of 322 

Bidwell Creek, hot springs on, description of 121-122 
Big Basin, carbonated spring in, description 

of 175 

Big Bend Hot Springs, description of 115-116 

Big Clipper Springs, description of 329 

Big Meadows, large cold springs in, descrip- 
tion of 330-331 

Bimini Hot Spring, description of 71, 72 

Bishop, hot spring near, description of 148 

Bitter Spring, description of 303 

Black Spring, description of 335 

Black Lake Springs, description of 336-337 

Blackrock Spring, description of 320-321 

Blancks Hot Springs, description of 104 

Blaney Meadows Hot Springs, description of. 54-55 

Blind Spring, description of 323 

Blodgett Magic Spring, description of 273, 274 

Blodgett Mineral Spring, description of 273-274 

Blue Lakes, sulphur spring near, description 

of 268 

Bodflsh Creek, sulphur spring on, descrip- 
tion of 272-273 

Bodie, warm springs near, description of. . '. 135-136 
Boiling point of water, relation of, to pressure 

and elevation 25 

403 



404 



INDEX. 



Bonanza Springs, description of 190 

Boonville, carbonated spring near, descrip- 
tion of 171 

Borate radicle, scarcity of, in spring waters . . 19 

Borego Spring, description of 349 

Boric acid, indication from, in spring waters. 19 

Bottle Spring, description of 334 

Box Spring, description of 352 

Box S Spring, description of 346 

Boyd Spring, description of 124 

Boyes Hot Springs, description of 112, 113 

Bradley Spring, description of 350-351 

Breeze Lalce, carbonated spring near, de- 

• scription of 241 

Bridgeport, hot springs near, description of. 133-135 

^Bridgeport, warm spf ings near, description 

;•■• of.. ...-•..;.. .....v.. J....---. 133,135-136 

Brockway Hot Springs,; description of 131 

Bromides, scarcity of, in spring waters 19 

Browns Creek, sulphur -springs on, deserip- 

'. tionof....-..!... 264 

Buckeye Hot Spring, description of 132-133 

Buckhorn Springs, description of 317-318 

Buckman Springs^ description of 247 

Bullion Mountains, svilphur springs near, de- 

r scription .of J ■.:.■.... 286 

Bumpass Hot Springs,- destription of. . 140-141,142 

plate showing 140 

Bundys Elsinore Hot Spring, descriptioii of. . 43 
Burney Creek, large cold springs on, descrip- 

... tionof. 328 

Burton Mound, sulphur springs on, descrip- 
tion of 277-278 

Butte County, list of springs in 372 

Bynum Spring, description of 182-183 

Byron Hot Springs, description of 109-112 

plate showing. ...... ....:...: 108 

^ saline springs at, description ct 293 

Bythinia Springs, description of 295, 296 

Cabin Springs, description of . •. 324 

Cactus Flat Spring,- description of 347 

Calaveras County,, spring in' 372 

€alciiun, source of, in water 17 

California, climatic and topographic extremes 

? in .,/.. 5-6 

f geologic map of ....-..•. In pocket. 

.•; map of, showing locations of hot, carbon- 

> ated, and sulphur springs In pocket. 

I, topographic map of. In pocket. 

California Hot Springs, description of 49-50 

Galistoga Hot Springs, description of 108-109 

Cameta Warm Spring, description of 77 

Campbell Hot Springs, cool springs at, de- 

• scription of. : 334 

description of, , 129-130 

Gantwell Soda Spring, description of 177 

Canyon Creek, warm springs near, description 

; of 120 

Carberry store, sulphur- spring near, descrip- 

.; tionof.. J.. ..'..:...... 281 

Carbon dioxide, source of, in spring waters. . . 1*9-20 
Carbon, sulphur spring near, description of. . 283 
Carbonate deposit, plates showing 124, 134 



Carbonated springs, descriptions of 155-248 

descriptions of, summary of 248-253 

Carbonated water, definition of 23 

value of 27 

Carbonates, source of, in water 18 

Carlsbad Springs, description of 187-188 

Carrizo Plain, sulphur spring in, description 

of 277 

Carrizo Springs, description of 349 

Casa Diablo Hot Pool, description of 147 

Casa Diablo Hot Springs, description of 146-147 

plate showing 140 

hot spring northeast of, description of 147 

Castalian Mineral Water, description of 304r-305 

Castle Crag Spring, description of ■ 224r-225 

Castle Creek, carbonated spring near, descrip- 
tion of 227 

sulphur spring on, description of 266 

Castle Hot Springs, description of 91-93 

Castle Rock Springs, description of 226-227 

Castle Springs, description of 222 

Cave Spring (Siskiyou County), description of 224 
Cave Springs (San Bernardino County), de- 
scription of 344 

Chalk Mountain, carbonated springs on, de- 
scription of 196-197 

springs near, description of 358 

Chaparral Spring, description of 356 

Chatsworth, sulphur spring near, description 

of 281 

Chicken-soup water, nature of 20 

China ranch springs, description of 343 

Chip Creek, carbonated springs on, descrip- 
tion of 230 

Chlorides, source of, in water 18 

Cisco, iron spring near, description of 313 

Clear Creek Hot Springs, description of. 51 

Clear Lake, carbonated springs near, descrip- 
tion of 180, 193, 196 

Coast Ranges, description of 7-11 

Coburn Soda Springs, description of 241-242 

Goes Spring, description of 214r-215 

Cole Creek, carbonated springs on, description 

of 186 

Colorado Desert, carbonated spring in, analy- 
sis of 248 

location of 14 

Color in spring waters, soiu-ce of 23-24 

Colusa County, list of springs in 372-373 

Colyear Springs, description of. 266 

Complexion Springs, description of 237-298 

Concentration of natural waters 21-22 

Congress Spring (Napa County), description 

of 156 

Congress Springs (Santa Clara County), de- 
scription of. 212,213 

Console Spring, description of 352 

Contra Costa County, list of springs in 373 

Cook Spring (Humboldt County), description 

of 261 

Cooks Springs (Colusa County), description 

of 204-205 

plate showing 200" 

Corn Springs, description of 348 

Corona Spring, description of 351-352 



INDEX. 



405 



Pago. 

Coso Hot Springs, description of 149-150 

vapor vents west of, description of 150-151 

Cottonwood Creek, South Fork of, sulpliur 

spring on, description of 267 

Cottonwood Spring (Inyo County), descrip- 
tion of 341 

Cottonwood Spring (San Bernardino County), 

description of 316 

Cottonwood Springs (Riverside County), de- 
scription of 348 

Crabtree Springs, description of 10:)-107 

Crook, J. K., cited 26 

Crow Creek, sulphur spring on, description of. 271 
Crystal Spring (Napa County), description of. 357 
Crystal Springs (Inyo County), description of. 339 
Cummings, sulphur springs near, description 

of 2o0 

Cushenbury Spring, description of 346-347 

D. 

Dante Springs, description of 344 

Davis Spring, description of 352 

Daylight Spring, description of 342-343 

Deadmans Holes, description of 303 

Deadshot Springs, description of 195 

Death Valley, location of 14 

Deep Creek, sulphur springs on branch of, d> 

scription of 258-259 

Deep Springs, description of 322 

Deerlick Springs, description of 261-263 

Deer Park Springs, description of 232-233 

Delonegha Springs , description of 51 

plate showing 50 

Deluz Warm Springs, description of 47-48 

Democrat Springs, description of 51-52 

Devils Kitchen, description of 141-142 

Dinsmore Soda Spring, description of 196 

Dolans Hot Spring, description of 57 

Dos Palmas Springs, description of 315 

Doyle Soda Springs, description of 242 

Drake Hot Springs, description of 142-143 

Duncan Springs, description of 167-168 

E. 

Eagle Lake, artesian springs near, descrip- 
tion of 326 

Eden Hot Springs, description of 37 

Eel River, sulphur spring near branch of, de- 
scription of 259 

El Pajaro Springs, description of 274-276 

Elder Creek, North Fork of, salt sprinj;s on, 

description of 299 

Eldorado County, list of springs in 373 

Electric spring water, explanation of 171-172 

Elgin Mine, hot springs at, description of . . 104^106 

El Granito Spring, description of 350 

Elizabeth Lake Canyon, warm springs in, de- 
scription of 66 

Elk Creek, salt springs near, description of... 299 

Elsinore Hot Springs, description of 42, 43 

El Tore Spring (Marin County), description 

of '. . . 255-256 

Emigrant Spring, description of 341 

Encino ranch, carbonated springs on, de- 
scription of 246-247 



Pago. 

England Springs, description of. 186 

Epsom Spring, description of 296 

Eureka, sulphur spring in, description of 260 

F- • : 

Fairview Hot Spring, description of 37, 

Fales Hot Springs, description of 13^ 

Fall River, springs at head of, description of 326-327 

Faults, distribution of , 14 

Feliz Creek, carbonated springs near, descrip- 
tion of 169 

Felts Springs, description of 300 

Fern Spring, description of 33& 

Ferndale Springs, description of 20& 

Fetters Hot Springs, description of 114 

plate showing , 108 

Figtree Johns Springs, description of 314-31J» 

Fish in spring waters 137| 

Fish Springs (Imperial County), description » 

of. .^ 3ia 

Fish Springs (Inyo County), description of. . 322 

Fish Valley, carbonated spring in, deserip- , 

tion of 23^ 

hot springs at head of, description of 51^ 

Florence Spring, description of 23^ 

Foerster Peak, carbonated spring near, de- , 

scription of 24^ 

Fountain Spring, description of 33^ 

Fonts Springs, description of 20^207, 

sulphur springs near, description of 26'^ 

Franz Valley, sulphur springs in, description j 

of 25^ 

Freeman Springs, description of 34Q 

Fresno County, list of springs in 373-37^ 

Fresno Hot Springs, description of 7^ 

Frink Springs, description of 34^ 

Furnace Creek ranch, salt springs near, de- 
scription of 30^ 

G. ■■ •♦ 

Gaillaumes Soda Springs, description of 162 

Garcia River, carbonated springs on, descrip- 
tion of. 170t-171 

Garlic Spring, description of ' 303 

Garretson Soda Springs, description of ■.216-217 

Geary Spring, description of * 335 

Gerber ranch, large cold springs on, descrip- 
tion of 329-330 

Geyser (Plumas County), description of. . . 143-144 

plate showing , " 50 

Geysers (Sonoma County), description of 83-88 

plate showing ....'...,...'... 146 

Gifford Springs, description of ......... 1 ,., . 357-358 

Gilroy Hot Spring, description of 79-80 

Glacier Spring, description of . . :' . , 33^ 

Glen Alpine Springs (Eldorado County), de- 
scription of .........: . 236-237 

Glen Alpine Springs (Lake County), deserip- ' 

tion of. 182 

Glen Ivy Hot Springs, description of 42 

Glenn County, list of spring? in.... "374 

Glennville, sulphur springs near,, description ' 

of ....: 286 

Gobbis Soda Spring, description of 17^ 

Goodman, Gertrude E., acknowledgments to 2& 
Gordon Hot Spring, description pf qS 



406 



INDEX. 



Granite Creek, East Fork of, carbonated 

springs on, description of 240 

Grant Spring, description of 212 

Grapevine Springs, description of 339-340 

Graves Spring, description of 353-354 

Great Springs, description of 328-329 

Great Central Valley, description of 11-12 

Grizzly Springs, description of 193-194 

plate showing 242 

Grovers Hot Springs, description of 131 

H. 

Haiwee, springs near, description of 339 

Halloran Springs, description of 344 

Harbin Springs, description of 93-95 

plate showing 92 

Hardness of water, nature of 23 

Harlem Hot Spring, description of 35,36 

Hay villa Sulphur Spring, description of 268 

Hazel Hill, carbonated springs at, description 

of 173 

Hazel Springs, description of 202 

Heath Soda Springs, description of 232 

Helms Soda Springs, description of 216 

Henderson Spring, description of 335 

Hensley Spring, description of 266-267 

Highland Springs, description of 183-185 

Highrock Spring, description of 128 

Hillydale Sulphur Spring, description of 271-272 

Hines Spring, description of 321 

Hinns Sulphur Spring, description of 272 

Hoaglin, sulphur spring near, description of . . 260 

Hoods Hot Springs, description of 82 

Hopland, artesian spring near, description of. 323 

Hoppins Springs, description of 201 

Horse Lake Valley, artesian springs in, 

description of 326 

Hot Creek, hot springs on, description of 119 

Hot Spring Valley, carbonated spring in, 

description of 227 

large cold springs in, description of 330 

Hot springs, deposits near 154-155 

descriptions of 32-151 

summary of 151-155 

rocks surrounding 154 

Hough Springs, description of 197-198 

plate showing 92 

Howard Springs, description of 95-96 

plate showing 92 

Huer Huero Springs, description of 277 

Humboldt Artesian Mineral Well, descrip- 
tion of 308-309 

Humboldt County, list of springs in 374 

Humbug Valley, carbonated spring in, de- 
scription of 230 

Hydrogen sulphide, source of , in spring waters 20 
Hydrogiobertite, deposit of 161-162 

I. 

Imperial County, list of springs in 374 

Indian Creek, carbonated springs on, descrip- 
tion of 228-229 

Indian Spring, description of 318 

Indian WellsSprings,descriptionof 340 

Inyo County, list of springs in 375-376 

Iodides, scarcity of, in spring waters 19 



Iron, source of, in water 17 

Iron Springs, descriptions of 312-313 

Isham Springs, description of 311,312 

J. 

Jackson Valley Mineral Springs, description 

of 176 

Jackson Valley Mud Springs, description of. 176-177 

plate showing 242 

Jacksons Napa Soda Springs, description 

of 155-156 

Jacumba Springs, description of 45 

Jones Hot Springs, description of 103 

Jordan Hot Springs, description of 53-54 

K. 
Kane Spring (Imperial County) description 

of 304 

Kane Springs (Kern County), description of. . 340 

Keane Spring, description of 343 

Keller Soda Spring, description of 217 

Kelly s Hot Spring, description of 1 18-1 19 

plate showing 50 

Kelseyville, carbonated wells at, description 

of 181 

Kentucky Springs, description of 353 

Kern County, list of springs in 376-377 

Kern River, North Fork of, carl onated 

spring near, description of 244-245 

Kemville, hot springs near, description of 50 

Kessler onyx marble quarry, salt springs 

near, description of 301 

Kessler Springs (San Luis Obispo County), 

description of 164-165 

Kessler Springs (San Bernardino County), 

description of 344 

Keystone Spring, description of 333 

Kinsner Soda Spring, description of 174-175 

Klamath Hot Springs, description of 120-121 

plate showing. 108 

Klamath Mountains, features of 8 

Klinefelter Springs, description of 345 

Koehn Springs , description of 340 

Kosk Creek, hot springs on, description of. . 116-117 
Kruger Spring, description of 128 

L. 

Lake County, list of springs in 377-379 

Lake Lahontan, analysis of dendritic tufa 

from 126 

Lake Tahoe, iron springs near, description of. 313 

water from, analysis of 22 

Lakeside Mineral Wells, description of 305 

La Mesa Spring, description of 350 

Lambert Soda Springs, description of 237-238 

Landers Spring, description of 336 

Large cold springs, descriptions of 326-333 

Las Cruces Hot Springs, description of 68 

Lassen County, list of springs in 379-380 

Lassen Peak region, map of 140 

Lava-covered region, description of 12 

Laytonville, sulphur spring near, descrip- 
tion of 259 

Leachs Springs, description of 343-344 

Le Conte Spring, description of 346 

Lee Soda Spring, description of 182 

Lithium, proportion of, in water 18 



INDEX. 



407 



Page. 

Little Blackrock Spring, description of 321 

Little Bogus Creek, carbonated springs near, 

description of 217-218 

Little Geysers, description of 88-89 

Little Hot Spring Valley, hot springs in, 

description of 118 

Little Lake, warm spring near, description 

of 148-149 

Little Shasta River, carbonated spring on, 

description of 219 

large cold springs near, description of 331 

Little Sulphur Creek, carbonated spring 

near, description of 166 

sulphurspring near, description of 258 

Little Sur River, North Fork of, hot springs 

on, description of 57 

Lloyd MeSHows, carbonated spring in, de- 
scription of 244 

Lone Willow Spring, description of 341-342 

Long Valley, warm springs in, description of. 147-148 
Long Valley Creek, carbonated springs near, 

description of 175,176 

Los Angeles County, list of springs in 380 

Los Guilicos Warm Springs, description of. . 114 
Lyons Spring (Ventura County), description 

of 278 

Lyons Springs (Lake County), description 

of 358-359 

Lytle Canyon, warm spring in, description of. 35 
Lytton Springs, description of 165-166 

M. 
McAlester ranch, springs on, description of. . . 355 

McCain Springs, description of 248 

McCloud, large cold springs near, description 

of 332 

McDowell Springs, description of 168-169 

McEwan ranch, warm springs on, descrip- 
tion of 114-115 

McLear Sulphur Spring, description of 283-284 

Madera County, list of springs in 381 

Madrone Spring, description of 214,215 

Magnesia Spring, description of 247-248 

Magnesie Springs, descriptions of 309-312 

Magnesium, source of, in water 17 

Manzanita mining property, hot springs on, 

description of 104 

Marble Hot Wells, description of 128-129 

Marin County, list of springs in 381 

Mariposa County, list of springs in 381 

Mark West Warm Springs, description of 115 

Martin Soda Spring, description of 219-220 

Mason ranch springs, description of 349 

Matilija Canyon, sulphur spring in, descrip- 
tion of 278 

Matilija Hot Springs, description of 63-04 

Mayhew Spring, description of 270-271 

Mendenhall, W. C, introduction by 5-6 

Mendenhall Springs, description of 309-310 

Mendocino County, list of springs In 381-383 

Mercey Hot Springs, description of 78-79 

Merrill, George P., cited 134 (footnote), 165 

Mesquite Spring, description of 346 

Mill Camp Springs, description of 348 

Minaret Creek, carbonated spring on, de- 
scription of 238 



Page. 
Mission Creek, sulphur spring on, description 

of 276 

Modoc County, list of springs in 383 

Mohave Desert, location of 14 

Monache Meadows, carbonated springs in, 

description of 246 

Mono Basin Warm Springs, description of. . 145-146 

Mono County, list of springs in 384 

Montague, large cold spring near, description 

of 331-332 

Montecito Hot Springs, description of 06-G7 

Monte Cristo Spring, description of 347 

Monterey County, list of springs in 384-385 

Moran Spring, description of 337 

Morgan Hot Springs, description of 138-139, 142 

Morton Soda Spring, description of 204 

Moss Spring, description of 335 

Mount Hamiah, springs at base of, descrip- 
tion of 358 

Mount Ida Spring, description of 230-231 

Mount Shasta, hot springs on, description of. . 144 

large cold springs on, description of 332-333 

Mountain Spring, description of 349 

Mountain View Spring, description of 260-261 

Mountaineer Creek, carbonated spring near, 

description of 244 

Mud Creek, large cold springs at head of, de- 
scription of 332 

Mud Spring (Alameda County), description 

of 355 

Mud Spring (Tehama County), description of 335 
Mud Spring, Jackson Valley (Mendocino 

County), description of 176-177 

Mud Volcanoes, description of 41-42 

Muir Springs, description of 259 

Mule Springs, description of 348 

Murrietta Hot Springs, description of 44 

X. 

Napa County, list of springs in 385 

Napa Rock Soda Springs, description of 161 

Napa Vichy Spring, description of 255 

Neills Hot Spring, description of 51 

Nelson Soda Springs, description of 243-244 

plate showing 242 

Nevada Coimty , spring in 385 

Newberry Spring, description of 317 

Newman Springs, description of 202 

Newsoms Arroyo Grande Warm Spring, de- 
scription of 68-69 

Neys Springs, description of 264-205 

Nitrate radicle, scarcity of, in spring waters. . . 19 
Nordhoff, sulphur spring near, da^cription 

of 278-279 

Nuvida Spring, description of 311-312 

O. 

Oasis, artesian springs at, description of 322 

Ocean water, analysis of 22 

O ' Donnell 's Springs , description of 256 

Odor in spring waters, source of 23 

Ohms Spring, description of 113 

Oil Spring, description of 194 

Old Woman Springs, description of 316 

Olive Spring, description of 272 



408 



INDEX. 



Page. 

Onyx marble, deposits of ,^ 133-135 , 

136, 162-163, 164-165, 221 

Orange County, list of springs in 385 

Ord Spring, description of 345 

Orestitnba Creek, sulphur springs on, descrip- 
tion of 271 

Organic matter, source of, in spring waters 20-21 

Ornbauns Mineral Spring, description of 170 

Orocopia Springs, description of 315-31G 

Orrs Hot Springs, description of 83 

plate showing 32 

Owens Lake, springs near, description of 339 

Owl Springs, description of 343 

Oxone Spring, description of 222 

P. 

Palm Springs, description of 40 

Palmdale Springs, description of 347 

Panamint Valley , warm spring in, description 

of 136 

Paoha Island, hot springs on, description of. 144^145 

sulphur spring on, description of 285-286 

Paradise Springs, description of 52-53 

Paraiso Hot Springs, description of 60-62 

plate showing — 32 

Paramore Spring, description of 203 

Paso Robles Hot Springs, description of. 72-73, 74-75 
Paso Robles Mud Bath Springs, description 

of 73-76 

Peach tree Springs, description of 355-356 

Peacock Spring, description of 346 

Pecho Warm Springs, description of 69-70 

Perennial springs, less known, descriptions 

of 359-371 

minor, descriptions of.' 333-371 

Petersons Mineral Spring, description of 177 

PhiUips Soda Springs, description of 161-162 

Phosphate radicle, scarcity of, in spring 

waters 19 

Piedmont Springs, description of 269-270 

Pilares Hot Spring, description of 40 

Pine Canyon, sulphur spring in, description 

of 270 

PittvUle, large cold spring near, description 

of 327-328 

Piute Spring, description of 345 

Placer County, list of springs in 385-386 

Plumas County, list of springs in 386-387 

Point Arena Hot Springs, description of 82-83 

Poison Spring, description of 302 

Potassium, source of, in water 17-18 

Pothole Spring, description of 334 

Powderhorn Creek, carbonated spring near, 

description of 233 

Pumice Flat, carbonated spring near, de- 
scription of 238 

Pvrit-" Spring, description of 356 

Q. 

Quigley Soda Springs, description of 195-196 

Quinn Horsecamp, carbonated spring near, 

description of 245 

R. 

Rabbit Springs, description of 316-317 

Radioactivity in waters, occurrence of 24 

Radium Sulphur Spring, description of 71-72 



Ranger Camp, carbonated spring near, de- 
scription of 203 

Rattlesnake Creek, warm springs near, de- 
scription of 120 

Reds Meadows Hot Springs, description of.. 55-56 

Resting Springs, description of 319-320 

Ricardo Springs, description of 340 

Richardson Springs, description of 291-293 

Rising River, description of 32S 

Ritchey Hot Springs, description of 39-40 

River Spring (Mono County), description of. 322 
River Spring (Tulare County), description of. 338 

Riverside County, list of springs in 387 

Rock Springs, description of 345 

Rock Creek, large cold springs on branch of 

(Plumas Coimty), description of. 331 
Rock Creek Springs (Shasta Coimty), descrip- 
tion of 329 

Rocky Point Spring, description of 80-81 

Rosamond, springs near, description of 354 

Rose Spring (Inyo Coimty), description of.. . 339 
Rose Spring (Los Angeles County), descrip- 
tion of 352-353 

Royal Spring, description of 202-203 

Rubicon River, sulphur springs on, descrip- 
tion of 285 

Rubicon Springs, description of 234-235 

Rush Creek, artesian springs near, descrip- 
tion of 325 

Russell, I. C, cited 125 

Russian River, carbonated springs on, de- 
scription of 170 

S. 

Sacramento River, water from, analysis of. . . 22 

Sacramento Valley, description of 11 

St. Helena White Sulphur Springs, descrip- 
tion of 254-255 

Saline Springs, descriptions of 289-309 

Saline Vallej^, warm spring in, description of. 136 

Saline waters, value of 27 

Salinity, grades of 22-23 

Salmon Creek Mineral Springs, description of. 174 

Salt Spring, description of 302-303 

Salt Spring Valley, salt spring in, description 

of 299 

Salton Sea, description of 41 (footnote) 

Samuel Soda Springs, description of 159-160 

San Benito County, well in 388 

San Benito Mineral Well, description of. . . 306-307 
San Bernardino County, list of springs in. . 388-389 

San Diego County, list of springs in 389-390 

San Jacinto Hot Springs, description of 38 

San Joaquin River, Middle Fork of, carbon- 
ated springs on, description of. . . 240 
North Fork of, carbonated spring on, de- 
scription of 240 

South Fork of, lower springs on, descrip- 
tion of 56 

San Joaquin Valley, description of 11 

San Juan Capistrano Hot Springs, descrip- 
tion of 48-49 

San Luis Hot Spring, description of 70-71 

San Luis Obispo County, list of springs in . . . 390 

San Marcos Hot Springs, description of 67-68 

Sand Spring, description of 342 

Santa Barbara County, list of springs in 391 



INDEX. 



409 



Page. 

Santa Barbara Springs, description of 295-296 

Santa Clara County, list of springs in 391 

Santa Cruz Coimty, list of springs in 392 

Santa Fe Springs, description of 282-283 

Santa Susana Mountains, sulphur spring in, 

description of 280 

Santa Ysabel Springs, description of 76-77 

Saragossa Spring, description of 3*17 

Saratoga Springs (Lake County), description 

of 179-180 

Saratoga Springs (San Bernardino Coimty j, 

description of 137-138 

Scott Creek, carbonated spring in canyon of, 

description of 182 

Scotty Springs, description of 338 

Searles Spring, description of 340 

Secret Springs, description of 325 

Seelys Spring, description of 321 

Seigler Springs, description of 96-98 

Sellicks Springs, description of 324 

Sereno Creek, carbonated spring near, descrip- 
tion of 232 

Serpentine areas, relation of springs to, de- 
scription of 203 

Sespe Hot Springs, description of 66 

Shaffer Hot Springs, description of 124-126 

Shasta County, list of springs in 392-393 

Shasta Springs, description of 220-221 

Shasta Valley, artesian springs in, descrip- 
tion of 323 

Sheep Springs, description of 325 

Shinns Peak, artesian springs near, descrip- 
tion of 325 

Shoemaker Dell, carbonated springs at, de- 
scription of 173 

Sierra Coimty, list of springs in 393 

Sierra Nevada, description of 12-13 

Sierran Mountains, approach of, to Coast 

Ranges 10-11 

Silica, source of, in water 17 

Stngleys Soda Spring, description of 171 

Siskiyou County, list of springs in 393-394 

Sisson, large cold springs near, description of. 332 

Sites, salt spring near, description of 298-299 

Skaggs Hot Springs, description of 81-82 

Slates Hot Springs, description of 56-57 

Smoke Creek, artesian springs near, descrip- 
tion of 325 

Snider ranch, carbonated spring on, descrip- 
tion of 175 

Soda Bar, carbonated springs at, description 

of 217 

Soda Bay Springs, description of 191-192 

Soda Creek (Shasta County), carbonated 

spring on, description of 225 

Soda Creek (Tulare County), carbonated 

spring on, description of 243 

Soda Spring Flat, carbonated springs in, de- 
scription of 239 

Soda Springs (Imperial County), description 

of 303 

Sodium, source of, in water 17-18 

Solano Coimty, list of springs in 394 

Sonoma County, list of springs in 394-395 

Soupan Hot Springs, description of 141 

carbonated spring north of, description of. 227 



Page. 

Southeastern desert region, description of 13-14 

Spanish Creek (Plumas County), carbonated 

springs on, description of 227-228 

Spanish Spring (Lassen County), description 

of 325 

Spiers Springs, description of 190-191 

Springs, classes of 30-31 

order of discussion of 31-32 

resorts at, table of 399-402 

table of, by counties 372-398 

Stabler, Herman, acknowledgments to 29 

Staininger raiich springs, description of 342 

Stanislaus County, list of springs in 395 

State Home at Eldridge, warm springs of, de- 
scription of 114 

Still ranch, springs on, description of 355 

Stingleys Hot Springs, description of 63 

Stonebreaker Hot Springs, description of. . 117-118 
String Meadows, spring near, description of. . 338 

Sulphates, source of, in water 18 

Sulphides, source of, in water 18 

Sulphur Bank, hot springs at, description of. 98-99 
Sulphur Creek, sulphur spring near, descrip- 
tion of 258 

Sulphur Meadows, sulphiu- spring in, de- 
scription of 286 

Sulphur Moimtain Springs, description of.. 279-280 

Sulphur springs, descriptions of 253-286 

description of, summary of 286-289 

Sulphur Valley, sulphur springs in, descrip- 
tion of 268 

Sulphureted water, definition of 23 

value of 27 

Summit Diggings, springs at, description of. 340 

Summit Soda Springs, description of 231-232 

Sunset Spring, description of 348 

Surprise Spring, description of 346 

Surprise Valley, hot springs in, description 

of 121-124 

Sweet Springs, description of 310-311 

T. 

Table Rock Spring, description of 219 

Tabulated data, explanation of 371 

Tamalpais Mineral Well, description of 307-308 

Tartarus Lake, description of 143 

Tassajara Hot Springs, description of 57-60 

Taylor Sulphur Spring, description of 256-257 

Tecopa, hot springs near, description of 137 

Tehama County, list of springs in 396 

Temblor ranch, springs on, description of 354 

Temperature of spring waters, causes of 24-25 

Texas Springs, description of 320 

Thermal waters, physiological effects of 28 

Thompson Spring, description of 354-355 

Three Springs, description of 338 

Tiptons Springs, description of 324-325 

Tolenas Springs, description of 162-163 

Tomaso Springs, description of 344 

Toro Springs (Riverside County), description 

"^of 314 

Travelers Home, carbonated spruigs at, de- 
scription of 174 

Travertine, deposits of 133-135, 136 

deposits of, plate showing 134 

Trinity County, list of .springs in 396 



410 



INDEX. 



Trinity River, Stewarts Fork of, salt springs 

on, description of 299 

Tucker ranch, sulphur spring on, description 

of.. 281 

Tufa, dendritic, analysis of 126 

dendritic, plate showing 124 

Tulare County, list of springs ia 396-397 

Tulare Lake, character of 11 

Tule River, Middle Fork of, carbonated spring 
on (Tulare County), description 

of 242 

South Fork of Middle Fork of, carbonated 
spring on (Tulare County), de- 
scription of 242-243 

Tule River Soda Spring (Tulare County), de- 
scription of 244 

Tule Springs (Inyo County), description of. . 342 

Tuolumne County, springs in 397 

Tuscan Springs, description of 289-291 

plate showing 200 

Twenty-nine Palms Springs, description of. . 316 

Twin Springs, description of 224 

U. 

Upper Funston Meadow, carbonated spring 

in, description of 245 

Upper Lake, carbonated wells near, descrip- 
tion of 180, 181 

Upper Soda Spring, description of 223 

Urbita Hot Springs, description of 36-37 

V. 

Vallecito Springs, description of 349 

Vallejo White Sulphur Spring, description of. 255 
Valley Spring (San Bernardino County), de- 
scription of 302 

Valley Springs (Calaveras County), descrip- 
tion of 300-301 

Ventura County, list of springs in 397-398 

Veronica Springs, description of 294-295, 296 

Veterans' Home, springs at, description of. . . 356 

Vichy Springs, description of 171-173 

Vickers Hot Springs, description of 62-63 

Victorville, spring near, description of 345 

Vontrigger Spring, description of 345 

W. 

Wall Springs, description of 257-258 

Walnut Creek, sulphur springs near, descrip- 
tion of 270 



Walters Mineral Springs, description of 159 

Warm Spring Valley, warm spring in, de- 
scription of 119-120 

Warm Springs, description of 80 

Warmcastle Soda Springs, description of 223 

Warner Hot Springs, description of 45-46 

Warrens Ranch Springs, description of 347 

Waterman Hot Springs, description of...„ 33,34,35 

Water, mineral, classification of 25-26 

mineral, properties of 22-24 

use of term 15 

pure, use of term 15 

substances in, source and amount of 17-21 

therapeutic value of 26-28 

Water Station Springs, description of 341 

Watts, W. L., cited 220-221 

Weed, W. H., cited, on algse in springs 20-21 

Weldon Valley, carbonated spring in, descrip- 
tion of 246 

Wendling, carbonated springs near, descrip- 
tion of 173 

Wentworth Springs, description of 235-236 

Wheelers Hot Springs, description of 64-66 

White ranch, carbonated spring on, descrip- 
tion of 175 

Wilbur Hot Springs, description of 99-103, 105 

plate showing 32 

Wild Rose Spring, description of 341 

Wiley ranch, carbonated springs on, descrip- 
tion of 198 

Williams Hot Springs, description of 52 

Willits, carbonated springs near, description 

of 175 

AVillow Spring (south of Portersville), de- 
scription of 336 

Willow Springs (near Rosamond), description 

of 318-319 

Witter Medical Springs, description of 177-179 

Y. 

Yankee Spring, description of 336 

Yosemite Valley, iron springs in. descripton 

of 312-313 

Yuba River, South Fork of, sulphur springs 

near, description of 284 

Yuha Spring, description of 304 

Z. 
Zem Zem Spring, description of , 268 



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WATER-SUPPLY PAPER 338 PLATE II 



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114" 



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Alluvium 

d lake deposits. I 
the State, areas of 

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42 



Granitic rocks 

{Including gneisses and schists) 



41 



40 




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